{"paper_id":"2bb533fb-edda-4fcb-a16d-91cc2b423a3a","body_text":"The ammonite faunas of the upper Hypselocyclum to Divisum zones (Lower Kimmeridgian, Upper Jurassic) at Małogoszcz, Holy Cross Mts., central Poland: their stratigraphical interpretation and evolutionary development | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Research Article The ammonite faunas of the upper Hypselocyclum to Divisum zones (Lower Kimmeridgian, Upper Jurassic) at Małogoszcz, Holy Cross Mts., central Poland: their stratigraphical interpretation and evolutionary development Andrzej Wierzbowski This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-4008521/v1 This work is licensed under a CC BY 4.0 License Status: Published Journal Publication published 26 Sep, 2024 Read the published version in Journal of Iberian Geology → Version 1 posted 5 You are reading this latest preprint version Abstract The transgressive succession of deposits of the late Early Kimmeridgian at Małogoszcz in the south-western margin of the Holy Cross Mts. in central Poland yielded diversified faunas of ammonites. The commonly represented Submediterranean ataxioceratid ammonites include the last members of Ataxioceras in the Hypselocyclum Zone and the assemblage of various Crussoliceras , Garnierisphinctes and Progeronia , mostly developed in the Divisum Zone, and associated upwards (Uhlandi Subzone) with aspidoceratids ( Pseudhimalayites ). A few typical Mediterranean ammonites ( Nebrodites , Presimoceras , Idoceras , Taramelliceras ) are indicative of the Herbichi Zone. The Subboreal ammonites include mostly Eurasenia , Involuticeras in addition to some Rasenia and Rasenioides of the uppermost Cymodoce Zone, corresponding to the Askepta Subzone. The changes in composition of ammonite faunas and comparison with the coeval faunas of other areas of Europe give indications on the evolutionary development of some Ataxiocertidae and Aulacostephanidae at the end of Early Kimmeridgian. The development of the Crussoliceras , Garnierisphinctes and Progeronia , having possibly their roots in the Mediterranean areas, was strictly correlated with the overall transgression and oscillations of sea-level controlled possibly by climatic eccentricity cycles in northern Tethyan shelf. This resulted also in decline of older Ataxioceras and its nearby allies. The indigenous lineage of Aulacostephanidae includes the transition from Eurasenia to Pararasenia. The development from Rasenioides to Aulacostephanoides occurred mostly in the Subboreal areas – although some late representatives of Rasenioides like R. moeschi reached the area of study. The existence of an independent lineage leading from Rasenia involuta to heavily-ribbed Aulacostephanoides/Aulacostephanus is also suggested. ammonites biostratigraphy correlations evolutionary faunal turnovers migrations Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 Introduction Geological setting . The Upper Jurassic deposits occurring around the Paleozoic core of the Holy Cross Mountains (Polish: Świętokrzyskie Mountains) in central Poland, in the north-eastern, the north-western and the south-western margins, represent remnants of the primary cover developed originally over the whole area. The lateral extent of the Upper Jurassic deposits was modified by Neo-Cimmerian (pre-Albian) tectonic movements and markedly changed by Laramian (at the end of Maastrichtian and during Palaeocene) uplift of the mountains which became the south-eastern fragment of the elevated zone of the Middle Polish Anticlinorium (Kutek & Głazek, 1972 ). The Upper Jurassic deposits are accessible for detailed study in several large quarries, including that of the Małogoszcz cement works in the south-western margin of the mountains (Fig. 1 ), where the detailed Kimmeridgian succession of carbonates has been described from (Matyja et al., 2006 ). The stratigraphical succession studied here, attaining about 25 meters in thickness, corresponds to the Skorków Lumachelle of Kutek ( 1968 ). It consists of oyster lumachelles, micritic limestones and marls rich in various fossils and oncoids representing the transgressive part of sedimentary sequence, covering the older shallow-water marls and sublithographic limestones deposited in restricted environment with a very poor fauna. The latter represent the final regressive fragment of an older sequence developed at the decline of the shallow-water carbonate platform (e.g., Kutek, 1994 ). A substantial fossil assemblage listed by Radwańska & Radwański (in: Matyja et al., 2006 ) comprises numerous bivalves (both deep infaunal to epifaunal oysters – such as Actinostreon and Nanogyra – forming mass accumulations), ammonites, brachiopods, lobsters, regular and irregular echinoids, starfish, crinoids and various fish remains, some of them bored by bryozoans and bivalves and/or encrusted by diverse epizoans such as serpulids and bryozoans. Materials and methodology . The ammonites occur fairly commonly. The collection of ammonites consisting of over 200 specimens determined to the genus level (and additionally in a large part to the species level) is composed of common representatives of three families: Ataxioceratidae, Aulacostephanidae and Aspidoceratidae, and rare ones of two others: Perisphinctidae and Oppeliidae. These ammonites have been picked during several years personally and donated by other persons during occasional visit in the quarry, being usually referred to the particular lithostratigraphical units (also after study of the matrix), but commonly without precise location therein. The most valuable specimens of the collection are housed in the Museum of the Geological Faculty of the University of Warsaw (collection number ZI/100). The dimorphism of ammonites, if strongly marked in shell morphology, is expressed morphotaxonomically both at the generic and species levels. This refers especially to the most commonly recognized forms of the families Ataxioceratidae and Aulacostephanidae whose taxonomical interpretation accepted herein is especially close to those presented by Atrops ( 1982 ) in relation to Ataxioceratidae, and by Wierzbowski ( 2022 ) in relation to Aulacostephanidae. Such an approach, although purely descriptive is “fully conscious”, because it makes easier study of evolutionary transformations in the lineages, especially those constraint by heterochrony, closely related to changes in environmental conditions. The whole succession studied can be subdivided into five units differing in lithology which along with stated differences in composition and preservation of faunal assemblages make possible recognition of the changes in the environmental conditions. Beside the chronostratigraphical interpretation of the succession, the composition and changes in ammonites faunas offer new data on their evolutionary development in relation to changing environment. Description of the lithological succession For the purpose of this study the whole succession of the Skorków Lumachelle at Małogoszcz is subdivided into five units A-E (see Fig. 2 ). The general faunal and lithological characters of the succession were given in several older studies (Kutek, 1968 ; Kaźmierczak & Pszczółkowski, 1968 ; Seilacher et al., 1985 ; Machalski, 1996; Matyja et al., 2006 ; Matyja, 2011 ), all of them have been taken into account along with some new observations when prepared the following description. Unit A consists of thick-bedded, soft bioclastic limestones with numerous internal moulds of various infaunal bivalves, including those of Pholadomya , often preserved in life-position. There occur also commonly epifaunal bivalves like Actinostreon , Trichites , Nanogyra and others, as well as various brachiopods and echinoids. The deposits attain 6.5 m in thickness. Their base is marked by the well-developed omission surface having character of hard-ground, and representing the successive stages of its development from soft- and firm-ground stages with numerous burrows ( Thalassinoides and Rhizocorallium ) to bivalve and polychaete borings, and encrustation by serpulids of the hard-ground stage. This level marks the lower boundary of the Skorków Lumachelle (or lumachelle/coquina formation) with the underlying “sublithographic” limestones of the Buczyna Limestone Mbr. of the Spinkowa Góra Fm. (Wierzbowski, 2020 ). Ammonite occur rather commonly, especially of the family Ataxioceratidae: Ataxioceras ( Parataxioceras ) to “ Orthosphinctes ( Ardescia )”, Crussoliceras , Garnierisphinctes and Progeronia , and of the family Aulacostephanidae: Eurasenia, Involuticeras, Prorasenia, Rasenia ( Pachypictonia ) (see Kutek, 1968 , 1994 ; Matyja, Wierzbowski, 2000 ; Wierzbowski, 2022 ; see also herein). Unit B consists of oyster lumachelles about 2.5 m in thickness. The lumachelles are composed of densely packed shells of Actinostreon (“ Lopha ”, “ Alectryonia ”) with marked admixture of other bivalve shells, and those of diverse other groups – brachiopods, gastropods, echinoids; additionally are found remains of starfish, crinoids, fish and others. The fossils are commonly overgrown by epizoans (sponges, serpulids, bryozoans) and bored by lithophags. The deposit reveals the features of non-deposition and winnowing of finer particles, as well as temporary reworking. The latter is shown e.g., by the occurrence of multiphase growth of oysters from the elongated forms attached to seminfaunal bivalve shells to the cup-shaped forms all of them preserved in deposit, but commonly not in life position; it is also the case of occurrence of disoriented internal moulds of deep burrowing bivalves, and clasts of coral colonies. All these features indicate the residual lag type character of the discussed deposit. The ammonites are fairly common – but usually fragmentarily preserved. These are especially represented by Ataxioceratidae: mostly Crussoliceras , Garnierisphinctes , less commonly Progeronia , but to the virtual absence of Ataxioceras and “ Orthosphinctes ”, and somewhat less abundantly by Aulacostephanidae: Eurasenia , Rasenia , Prorasenia (see Kutek, 1968 , 1994 ; Matyja, Wierzbowski, 2000 ; Wierzbowski, 2022 , see also herein). Unit C having only 1.75 m in thickness is developed as oncolitic limestone. Oncolites differ markedly in final size from less than millimeter to 3–4 cm, but the most commonly around 0.5-1 cm in diameter. The associated fauna is represented mostly by various bivalves, both infaunal to seminfaunal (often preserved in life position, such as Pleuromya ) and epifaunal types (especially Nanogyra ), associated with brachiopods, gastropods and echinoids. The ammonites occur fairly commonly. There is observed a marked domination of Ataxioceratidae: Crussoliceras , Garnierisphinctes , and Progeronia , and less common occurrence of Aulacostephanidae: mostly Prorasenia , subordinately Involuticeras and Eurasenia , but also of Aspidoceratidae: Pseudhimalayites and Psedowaagenia (see detailed comments below). Unit D, attaining 8.25 m in thickness, consists of lumachelles with Nanogyra : these are composed of Nanogyra shells and their hash occurring in micritic limestone or marly matrix; the deposits are well-bedded with intervening beds of micritic limestones and marls, especially common in the middle part of the unit. The faunal assemblage is rather monotonous, dominated by epifaunal oysters Nanogyra , less commonly serpulids, crinoids, echinoids, starfish. The overlying deposits of unit E, 5.50 m in thickness, are thick-bedded bioclastic limestones with numerous internal moulds of various infaunal bivalves, including those of Pholadomya , intervening in the middle by a prominent marly bed without macrofana. A highest bed of limestones of unit E yielded numerous specimens of aspidoceratid ammonite Pseudhimalayites. The collection of ammonites coming from units D and E is, however, treated jointly, because of difficulties in proper location of some collected ammonites. It is composed of occurring mostly in nearly equal proportions Ataxioceratidae ( Crussoliceras , Garnierisphinctes , Tolvericeras , Progeronia ) and Aspidoceras ( Pseudhimalayites , very commonly). Some specimens of Aulacostephanidae represent a very diversified assemblage ( Prorasenia , Rasenia , Rasenioides , and possibly Pararasenia ) (Kutek, 1968 ; Matyja, Wierzbowski, 2000 ; Wierzbowski, 2022 ; see also comments below). A few large specimens of phylloceratids attaining about 0.5 m in diameter discovered in an upper part of unit E represent possibly allochtonous post-mortem drifted shells. Stratigraphical and palaeobiogeographical interpretation of the ammonite faunas The studied ammonite faunas contain besides the dominating Submediterranean-Mediterranean forms, also fairly commonly the Subboreal ones, as well as some of the strictly Mediterranean origin. Such a spectrum of ammonites enables not only the recognition of the various biostratigraphical zonations, but also makes possible correlation between the particular zonal schemes of different bioprovinces. The ammonites of the family Ataxioceratidae are the typical Submediterranean (partly also Mediterranean) forms. Although “the family is still one of the most difficult to classify” ( Enay & Howarth, 2019 , p. 112; see also discussion in chapter on evolution), its differentiation has became the basis for foundation of the Submediterranean zonations of the Lower Kimmeridgian, especially that established in south-eastern France, in the Jura Mts. in Switzerland, and in Swabian Alb and Franconian Alb in southern Germany (see e.g., Geyer, 1961 ; Atrops, 1982 ; Gygi, 2003 ; Enay et al., 2014 ), which is evidently recognizable in the area of central Poland (e.g., Kutek, 1968 ), including the section studied. The ammonites studied herein can be attributed to three different groups. The first of them recognized only in unit A in the Małogoszcz section is closely related to the genus Ataxioceras. It is represented by Ataxioceras ( Parataxioceras ) cf. planulatum (Quenstedt) (Fig. 3 a), A. ( P. ) oppeli parvum Atrops (Fig. 3 b), and “ Orthosphinctes ( Ardescia )” perayensis Atrops (Fig. 3 c). The representatives of Ataxioceras are indicative of the semistriatum horizon, possibly beginning from its base as suggests occurrence of a form similar to A. planulatum characteristic of still older hypselocyclum horizon, of the upper part of the Lothari Subzone of the Hypselocyclum Zone in the accepted herein subdivision of Atrops ( 1982 ). The occurrence of “ O ”. perayensis , being a form of the Ataxioceras ( Parataxioceras ) oppeli group, possibly reduced in ontogenetic development due to the heterochrony, is indicative moreover of the topmost part of the Hypselocyclum Zone (Atrops, 1982 ; see also comments on evolution below). The stratigraphical interpretation of all these ammonites is consistent with the occurrence of Crussoliceras and Garnierisphinctes of the second group of Ataxioceratidae in the discussed ammonite fauna of unit A. Both these genera appear for the first time in the Submediterranean succession in the semistriatum horizon of the Hypselocyclum Zone (Atrops, 1982 ). Of the recognized here three species of that group – G. melliconense (Geyer) (Fig. 3 d), Crussoliceras sayni (Camus et Thieuloy) (Fig. 4 a), and Garnierisphinctes garnieri (Fontannes) (Fig. 4 b)– the middle has been reported from the upper part of the Lothari Subzone (Gygi, 2003 ), whereas the level of appearance of the latter two has not been so far precisely recognized. The genus Progeronia of the third group of Ataxioceratidae is represented in unit A both by macroconchs: Progeronia ( Progeronia ) progeron (von Ammon) (Fig. 5 a) and P. ( P. ) cf. eggeri (von Ammon), and microconch Progeronia ( Hugueninsphinctes ) breviceps (Quenstedt) (Fig. 5 b). Although the appearance of Progeronia in the upper part of the Hypselocyclum Zone has been commonly recognized (e.g., Atrops, 1982 ), the reported new findings for the first time firmly prove the occurrence of the discussed species at that stratigraphical level. The ammonites coming from unit B do not reveal the representatives of the first group related to the genus Ataxioceras. Instead there are commonly represented forms of two other groups of Ataxioceratidae: Crussoliceras and Garnierisphinctes ones, as well as that of the genus Progeronia. Unfortunately because of the taphonomic reasons (see above) the specimens are mostly incomplete and difficult for closer determination. The only recognized specifically forms are: Garnieriphinctes cf. garnieri (Fontannes) (Fig. 3 e) and Crussoliceras cf. aceroides Geyer (Fig. 4 c-d). Nevertheless, the assemblage is diagnostic of the lower part of the Divisum Zone – and may be treated as corresponding to the Crusoliensis or Tenuicostatum Subzone according to stratigraphical interpretation accepted herein (see e.g., Atrops, 1982 ; Enay et al., 2014 ). It should be remembered, however, that in stratigraphical scheme of similar Submediterranean succession of southern Germany, the lower boundary of the Divisum Zone has been originally correlated with the level of the first occurrence of Crussoliceras and Garnierisphinctes (e.g., Geyer, 1961 ). According to that stratigrapical subdivision, the whole interval corresponding to unit A in the Małogoszcz section (compared with the upper part of the Lothari Subzone herein) would be correlated already with the lowest part of the Divisum Zone. On the other hand, a markedly different ammonite succession is recognized in the coeval deposits of the Spanish sections of the Iberian Range, which can treated as representative of the western part of Submediterranean Province. It includes the occurrence there of a special ataxiocertid group distinguished as corresponding to the new genus Geyericeras , not known in other European areas. These ammonites define the aragoniense stratigraphical horizon occurring directly below the appearance of Crussoliceras indicating already the base of the Divisum Zone. The relevant correlation with SE France and eastern parts of the Submediterranean Province, including central Poland, strongly suggests the position of the aragoniense horizon directly below the upper part of the semistriatum horizon and the perayensis horizon (see Moliner & Olóriz, 2009 , 2010 ; see also Moliner, 2009 ). The ataxioceratid ammonites from unit C of the Małogoszcz section are still markedly dominated by Garnierishinctes and Crussoliceras , although the species are mostly different when compared with older units: Garnierisphinctes semigarnieri (Geyer) (Fig. 6 a), G. championneti (Fontannes) (Fig. 6 b), G. plebejus (Neumayr) (Fig. 6 c), as well as Crussoliceras cf. lacertosum (Fontannes), C. cf. atavum (Schneid) – aceroides (Geyer). It is worth noting also the first occurrence of a form which possibly can be referred to the genus Tolvericeras ; the corresponding specimens (Fig. 6 d) are very similar to that described as “ Tolvericeras ( Tolvericeras ) n. sp.” by Gygi ( 2003 , Figs. 165–166) showing the polygyrate subdivision of ribs placed low in the whorl-side; this form was treated subsequently as taking the intermediate position between Garnierisphinctes and Tolvericeras (Enay et al., 2014 , p. 327). Some representatives of Progeronia with well preserved specimen of Progeronia ( Hugueninsphinctes ) breviceps (Quenstedt) (Fig. 5 c) are also recognized. The occurrence of several specimens of Aspidoceratidae represented mostly by Pseudohimalayites uhlandi (Oppel) unequivocally indicates that the whole ammonite assemblage from unit C corresponds already to the Uhlandi Subzone of the upper part of the Divisum Zone (see e.g., Geyer, 1961 ). The last ataxioceratid ammonites coming from units D and E are dominated by representatives of Crussoliceras : C. cf. crusoliense (Fontannes); Garnierisphinctes : G. championneti (Fontannes); and Tolvericeras group; the representatives of the Progeronia group: Progeronia ( Progeronia ) cf. eggeri (von Ammon) (Fig. 5 d) are less common. On the other hand, very numerously occur Aspidoceratidae represented almost exclusively by Psudhimalayites uhlandi (Oppel). These ammonites represent the upper parts of the Uhlandi Subzone of the Divisum Zone. Several ammonites of the families Ataxioceratidae (such as Crussoliceras , Garnierisphinctes and Progeronia ), as well as of Aspidoceratidae (mostly Pseudhimalayites ) occurring in the studied succession of the Holy Cross Mts., central Poland, are in common with areas of the Mediterranean Province such as the Venetian Alps (see e.g., Pavia et al., 1987 ; Sarti, 1993 ; Caracuel et al., 1998 ), and the Central Appenines (Cecca et al., 1985 ; Cecca & Santantonio, 1986 ) in Italy, the Betic Cordillera in southern Spain (Olóriz, 1978 ), the Gerecse-Pils Moutains and the Bakony Mountains in Hungary (Főzy & Scherzinger, 2013 ; Főzy et al., 2022 ), the Romanian Carpathians (e.g., Grigore, 2000 ), and the Balkan Mts. in Bulgaria (Sapunov, 1979 ). This along with occurrence in the succession studied of some strictly Tethyan ammonites, such as Presimoceras , Idoceras and Nebrodites allows for recognition of the Mediterranean zonation (see Sarti, 1993 ; Caracuel et al., 1998 , and correlations with older subdivisions). The ammonites of the genus Presimoceras occur rarely in unit B of the Małogoszcz section. They are fragmentarily preserved, nevertheless they can be attributed to the P. herbichi group (Fig. 7 g-h-i), being possibly close to P. nodulatum (Quenstedt). Such taxonomical interpretation indicates the correlation with the Mediterranean Herbichi Zone, additionally because of common occurrence of Crussoliceras - with its middle part – the Divisum Subzone (see Sarti, 1993 ). The occurrence of a single specimen of Idoceras balderum (Oppel) (Fig. 7 k) in the discussed unit B suggests also similar correlation. Although the typical forms of I. balderum are commonly referred to the upper part of the Divisum Zone in Submediterranean Province (SE France, southern Germany, see e.g., Geyer, 1961 ; Atrops, 1982 ; see also Schweigert & Kuschel, 2017 ), some specimens coming from a lower part of the Divisum Zone in other areas (Swiss Jura Mts., Venetian Alps, Italy) are compared with that species as well (see e.g., Gygi & Persoz, 1986 ; Pavia et al., 1987 ; Sarti, 1993 ). The overlying deposits of unit C yielded a few specimens of Nebrodites including N. favaraenenis (Gemmellaro) (Fig. 7 f) and N. cf. agrigentinus (Gemmellaro) (Fig. 7 j), which together with appearance of Pseudhimalayites uhlandi (Oppel) indicate the upper part of the Herbichi Zone – the Uhlandi Subzone (see Sarti, 1993 ). Similarly, the co-occurrence of P. uhlandi with Nebrodites sp. and Taramelliceras ( Taramelliceras ) compsum (Oppel) (Fig. 7 l) as recognized in still higher units units D and E indicates the presence of some upper parts of the Uhlandi Subzone (see Caracuel et al., 1998 ). Some problem arises with interpretation in term of the Mediterranean zonation of the lowest part of the studied succession – unit A of the Małogoszcz section, corresponding in the Submediterranean subdivision to the uppermost part of the Hypselocyclum Zone and the upper part of the Lothari Subzone. The only ammonite of a strictly Mediterranean character coming from that stratigraphical interval is Nebrodites maccerimus (Quenstedt) (Fig. 7 e), according to interpretation of the species by Ziegler (1959). Just that species was reported, however, from the boundary beds of the two Mediterranean zones – the Strombecki Zone and the Herbichi Zone or corresponding beds of the Divisum Zone (Caracuel et al., 1998 ; see also Olóriz, 1978 ; Sapunov, 1979 ). This, together with observations given above, suggests the discussed unit A corresponds most probably to the lowermost part of the Herbichi Zone. The ammonite faunas of the family Aulacostephanidae commonly represented in the succession studied are indicative of the Subboreal Province. These ammonites numerously occurring in units A to B, less commonly in unit C, are mostly belonging to the genera Eurasenia and Involuticeras of the north-eastern European branch of the family, and rarely to the genus Rasenia (and its local ally Pachypictonia ) related to its north-western European branch (Wierzbowski, 2022 ); both these groups of macroconchs occur together with their microconch counterparts of the genus Prorasenia . Some of these ammonites were presented and discussed previously: Rasenia ( Pachypictonia ) aff. indicatoria (Schneid), which seems to be related to Rasenia evoluta Spath (Wierzbowski, 2022 , pl. 7), Eurasenia rolandi (Oppel) (Wierzbowski, 2022 , pl. 10:4), and E. trimera (Oppel) (Wierzbowski, 2022 , pl. 11: 4) as well as Involuticeras involutum (Quenstedt) (Wierzbowski, 2022 , pl. 14: 2) – all of them from unit A; Eurasenia pendula (Schneid) (Wierzbowski, 2022 , pl. 11: 2–3) – from unit B; and Eurasenia trimera (Oppel) (Wierzbowski, 2022 , pl. 11: 5), possibly from unit C. In addition, several specimens of E. trimera (Oppel), E. trifurcata (Reinecke), E. pendula (Schneid), associated with Involuticeras , including I. crassicostatum (Geyer), along with common Prorasenia – especially P. quenstedti Schindewolf and P. witteana (Oppel), are reported from units A to C. On the other hand, some specimens of the genus Rasenia , including form similar to R. involuta Spath (Fig. 7 a-b), have been recognized in units B and D-E (near the top of the section). Summarizing, the ammonites of the genera Eurasenia and Involuticeras (associated with Prorasenia microconchs) occur in units A-C in the Małogoszcz section, indicating a stronger NE Subboreal influences, whereas NW Subboreal Rasenia are sporadically encountered nearly throughout the whole succession up to its top. Additionally, a few fragmentarily preserved specimens from unit E (and possibly its upper part), showing the ribbing similar to that of Eurasenia , reveal some weakening of ornamentation on the ventral side of whorls resembling thus younger genus Pararasenia (see Ziegler, 1962 ). They are especially similar to P. quenstedti Durand, differing in more elongated primary ribs, and in a weaker development of the ventral smooth band: thus, they are referred herein to as ? Pararasenia aff. quenstedti Durand (Fig. 7 c-d). Moreover, in the upper part of the succession there appear rarely ammonites of the genus Rasenioides , representing a different branch of Aulacostephanidae, such as R. moeschi (Oppel), coming from the lowermost part of unit D, and illustrated by Matyja & Wierzbowski ( 2000 , Fig. 4 c) and Wierzbowski ( 2022 , pl. 15:2A-B), and some other poorly preserved and difficult for closer determination specimens of that genus currently recognized in units D-E. The stratigraphical interpretation of the discussed Subboreal ammonites in term of the Subboreal zonation indicates the correlation of the whole discussed succession with the NW European Cymodoce Zone. The occurrence of ammonites similar to Rasenia evoluta and R. involuta , strongly suggests the presence of the higher levels of that zone (see Birkelund et al., 1978 , 1983 ). It should be remembered, however, that the highest part of the Cymodoce Zone was often treated in the past as an interval characterized by common occurrence of the fine-ribbed Rasenioides. In the studied succession at Małogoszcz, dominated by Submediterranean ammonites, the Subboreal Rasenioides ammonites are very rare, which precludes the precise differentiation of stratigraphical intervals corresponding to the Askepta Subzone, and/or Chatelaillonensis Subzone – both defined by occurrence of the Rasenioides faunas in northern European areas (see Birkelund et al., 1983 ; Hantzpergue, 1989 , 1995 ). The former can be possibly correlated with the bulk of the succession studied from the Submediterranean horizon perayensis at its base, whereas the base of the latter subzone runs possibly somewhat lower, near the base of the semistriatum horizon, as resulted from wider biostratigraphical correlations of the Subboreal and Submediterranean sections (see Matyja, Wierzbowski, 2000 ; Comment et al., 2015 ). Changes in environment versus evolutionary development of ammonites The stratigraphical interval corresponding to the upper part of the Hypselocyclum Zone and to the Divisum Zone (or in a broader sense to the whole Divisum Zone) of the uppermost Lower Kimmeridgian represents one of the most prominent faunal turnover in the whole Upper Jurassic. It is markedly correlated with changes in the depositional environment as based on sedimentological data. The main reasons of changes were of climatic and tectonic nature resulting from sea-level oscillations, and/or opening of new sea-routs. It should be remembered that the deepest faunal changes generally occurred during the transgressions, whereas endemism was rather related to dominance of the shallow-water environments (Atrops & Ferry, 1989 ; Hanzpergue, 1995; Wierzbowski, 2022 ). The stratigraphical interval discussed herein corresponded in the Submediterranean Province to decline of the shallow-water carbonate platforms due to progress of a large transgression. This resulted from the tectonic subsidence of the wide shallow-water carbonate areas including that of the Holy Cross Mountains in central Poland: at the boundary between the COK and the LUK tectono-stratigraphic sequences (Kutek, 1994 ) which corresponds to the boundary between the Buczyna Mbr. of the Spinkowa Góra Fm., and the Skorków Lumachelle of the Coquina Fm. in the Małogoszcz section (Wierzbowski, 2020 ). The progress of the transgression is well shown in the section studied by several sedimentological observation summarized by Matyja et al. ( 2006 ), and by analysis of the geochemical data, mostly oxygen and carbon composition of shells of various oysters by Wierzbowski ( 2019 ). A similar tectonic phenomenon is observed in the development of the Banné Member of the Lower Reuchenette Fm. in the Jura Mountains of northern Switzerland which marks the change from an older flat carbonate platform topography into that of a “prominent basin and swell morphology” (Jank et al., 2006 ). In addition, the climatic oscillations had also a marked influence on sea-level changes, especially those of longer duration related to 100-kyr and 405-kyr eccentricity cycles. Such a study to attempt to recognize the climatic cycles was presented on the basis of detailed geochemical analysis of the Early Kimmeridgian pelagic deposits of the south-eastern France having a good ammonite stratigraphy (Boulila et al., 2008 ; see also Atrops, 1982 ). It resulted in recognition of three main eccentricity cycles within deposits strictly coeval to those studied herein and showing similar assemblage of ammonites: beginning with the important transgressive level corresponding to minimum of 405-kyr MS cycle developed at the base of the whole succession (Min. 4 in Fig. 2 of Boulila et al., 2008 ), and the following two minima of 100-kyr cycles. The duration of the whole stratigraphical interval corresponding to the broadly treated Divisum Zone can be estimated as 260 to 300 kyr (Boulila et al., 2008 ). The overall transgression at the decline of the Early Kimmeridgian attained its very high level in central Poland (and south-eastern France) at the end of the Hypselocyclum Chron – during the semistriatum and perayenis horizons, when the transgressive deposits of a basal part of the Skorków Lumachelle (denoted herein as unit A, see Fig. 2 ) completely covered the earlier shallow-water carbonate platform deposits. This level additionally corresponds to the minimum (Min. 4 after Boulila et al., 2008 ) of the 405-kyr eccentricity cycle: it marks the minimum of the magnetic susceptibility (MS), and corresponds to enhanced carbonate production, showing the maximum insolation, which appears to have induced a very high sea-level according to the model proposed by Boulila et al. ( 2008 , 2010 ). The transgression in the Submediterranean Province controlled both by climatic and synsedimentary tectonics resulted in a marked exchange of the ammonite faunas (Fig. 8 ). The extinction of the older lineage of typical Submediterranean ammonites Ataxioceratinae, corresponding to decline of the genus Ataxioceras , was associated with the appearance of new members of the family Ataxioceratidae, such as genera Crussoliceras and Garnierisphinctes , beginning a new evolutionary stage of their development (see Atrops & Ferry, 1989 ; Enay & Howarth, 2019 ). The former lineage is represented in the studied interval of the uppermost Hypselocyclum Zone of the Submediterranean Province, from south-eastern France to central Poland, by the last smaller-sized forms of the genus Ataxioceras , both micro- and macroconchs (Atrops, 1982 ). The final, somewhat isolated microconch member of that lineage is “ Orthosphinctes ( Ardescia )” perayensis Atrops. This form has been sometimes treated as the end-member of the separate Ardescia lineage (or even Lithacosphinctes lineage; see Moliner & Olóriz, 2010 ), but it can be also considered as the final member of the small-sized Ataxioceras ( Parataxioceras ) oppeli group, originated due to the heterochrony process. It may be concluded thus, it is possibly a small-sized form developed due to progenesis as shown by its ornamentation very similar to that of the inner whorls of its direct forerunner – the subspecies A. ( P. ) oppeli parvum Atrops (see also Atrops, 1982 , p. 228, Fig. 53). When discussing the phylogenetical position of the genus Crussoliceras the most commonly interpretation given (Hantzpergue, 1989 ; see also Enay et al., 2014 ) suggested its origin from the Early Kimmeridgian Lithacosphinctes due to growth heterochrony – mostly progenesis and neoteny. The genus Lithacosphinctes as interpreted recently (e.g., Moliner & Olóriz, 2010 ) includes both micro- and macroconchs corresponding to “the most conservative lineage” among the Early Kimmeridgian Submediterranean Ataxioceratinae: according to such interpretation the genus comprises also some evolute, smaller-sized microconch species occurring in the lower part of the Lothari Subzone, at the end of the lineage, and attributed previously to the Orthosphinctes ( Ardescia ) inconditus group (see Atrops, 1982 ), but excluding “ O. ( A. )” perayensis as shown herein (see above). However, in accordance to that, there does not exist any link in the Submediterranean successions, both stratigraphical and morphological nature, between the older Lithacosphinctes group, and the younger well-developed Crussoliceras group. It is the reason that the proposed lineage of evolutionary development from the indigenous Submediterranean genus Lithacosphinctes to the suddenly appearing genus Crussoliceras is not accepted herein. It should be remembered that according to Moliner ( 2010 ), the genus Garnierisphinctes has been treated as descendent of a special group of the genus Ardescia (recognized as the separate genus, composed both of micro-and macroconchs), and moreover it was suggested that the genus Progeronia evolved from Garnierisphinctes during the late Divisum Chron. Also that interpretation is not accepted because of the stratigraphical reasons – the occurrence of the typical representatives of the genus Progeronia in much older deposits of the Early Kimmeridgian (see assemblage of unit A herein, see also e.g., Sarti, 1993 ). The new ammonite genera – Crussoliceras , Garnierisphinctes and Progeronia which appeared during discussed transgression at the end of the Hypselocyclum Chron have had possibly their roots in the Mediterranean areas. Such an opinion was expressed already by Pavia et al. ( 1987 ) who suggested affinity of Crussoliceras to the Mediterranean Passendorferiinae, which interpretation has been, however, partly questioned by Enay et al. ( 2014 ). The Mediterranean origin of the discussed genera can be, however, additionally supported by the occurrence of the genera Progeronia and possibly Crussoliceras deep in the Mediterranean Strombecki Zone – correlated with some lower parts of the Submediterranean Hypselocyclum Zone, markedly below the Lothari Subzone (see e.g., Sarti, 1993 ). The principal reason for suggesting that representatives of the genera Crussoliceras and Garnierisphinctes have been originated from Mediterranean migrants is, however, that there are not known their earlier Submediterranean forerunners. Somewhat different situation is with the genus Progeronia only, because there are known some forms occurring in older deposits of the Submediterranean succession which seem similar to typical representatives of the genus – e.g., such as “ Orthoshinctes ( Ardescia )” enayi Atrops occurring at the narrow interval between the lower and middle parts of the Platynota Zone from SE France to central Poland (Atrops, 1982 ; see also Wierzbowski, 2017 ). The open problem is, however, if they represent the fragmentarily recognized members of a single (?Mediterranean) lineage, or the local offshoots of Ataxioceratidae developed during the transgressive episodes. A generally poor knowledge on details of the succession (and their precise dating) yielding ammonites referred to as Orthosphinctes, Crussoliceras and Progeronia (e.g., Pavia et al., 1987 ; Sarti, 1993 ) in the crucial intervals of the Lower Kimmeridgian (mostly the Strombecki Zone) in the Mediterranean sections prevents the detailed recognition of the evolutionary development of the discussed lineages. The evolutionary development of ammonites of the family Aulacostephanidae proceeded a different way. In central Poland, in the area of Burzenin, north-west of the Holy Cross Mountains, in the deposits of open-marine environment of the middle part of the Hypselocyclum Zone (i.e. older than studied herein), was noted a marked increase in number, and in morphological development of representatives of the family (Wierzbowski, 2017 ). These ammonites belonged here to two different groups: that showing a more heavily-ribbed shells and representing possibly a more shallow-water environment such as Eurasenia and Involuticeras , and another one composed of Vineta to Balticeras and the first Rasenioides showing more subdued ribbing, exploring possibly more-open marine, nektonic environment (Wierzbowski, 2022 ). The overall transgression at the end of the Hypselocyclum Chron brought the heavily-ribbed Aulacostephanidae into flooded area of the shallow-water carbonate platform of the Holy Cross Mountains. Their share within the whole ammonite fauna of unit A in the Małogoszcz section ranges even up to about 35%. On the other hand, the aulacostephanids of the second group were totally absent in this area. Similar features of distribution of ammonites of the family Aulacostephanidae have been observed also in other shallow-water areas of the Western European Shelf, corresponding to the so-called “Western European Swell” (Hantzpergue, 1989 ; Hantzpergue et al., 1997 ; see also Enay et al., 2014 ). A sudden appearance of ammonites of the genus Eurasenia , along and above the occurrence of Ataxioceras of A. lothari group, “coincided with a maximum sea-level rise” (Hantzpergue, 1995 , p. 247). The horizons aulsnisa and manicata as defined on the basis of Eurasenia in the Western European Shelf can be just correlated with the semistriatum horizon of the upper part of the Hypselocyclum Zone of the Submediterranean zonation (Hantzpergue, 1989 ; Matyja & Wierzbowski, 2000 ). On the other hand, a sudden development of the genus Rasenioides representing the second group of Aulacostephanidae took place in the areas of northern and north-western Europe corresponding to the Subboreal Province, or representing the transitional areas between Submediterranean and Subboreal provinces. The dominance of these ammonites is observed e.g., in England (Birkelund et al., 1983 ), where their appearance defines the base of the Askepta Subzone correlated with the upper part of the Subboreal Cymodoce Zone, but also in a similar stratigraphical position in the Peri-Baltic Syneclise from the north-eastern Poland to Lithuania (e.g., Wierzbowski et al., 2015 ). In Aquitaine (Hantzpergue, 1989 ; Hantzpergue et al., 1997 ), the appearance of Rasenioides defines the base of the askeptus horizon within the Chatelaillonensis Subzone – which is located directly above the aulsnisa-manicata horizons with Eurasenia. The crucial for correlation of the discussed aulacostephanid (Subboreal) and the ataxioceratid (Submediterranean) zonations appeared the data from boreholes in the Zalesie Anticline in northern Poland studied by the present author. The recognized here (Matyja & Wierzbowski, 2000 , Figs. 3 – 4 ) nearly coeval occurrence of early Rasenioides and “ Orthosphinctes ( Ardescia )” perayensis Atrops indicates, the correlation of the lowermost part of the Askepta Subzone or askeptus horizon of the Chatelaillonensis Subzone in Subboreal or transitional areas of the northern Europe with the perayensis horizon of the uppermost part of the Hypselocylum Zone of the Submediterranean Province. It should be remembered, however, that the occurrence of “ O. ( A. )” perayensis along with late representatives of the genus Rasenioides transitional to Aulacostephanoides , as reported in archival materials from core Kcynia IG-IV in northern Poland (Matyja & Wierzbowski, 2000 , Fig. 2 ), suggests also a local higher upward range of that species. Anyway, the sudden invasion of the the Subboreal Rasenioides to the north, coincided possibly in time with a sudden spread across the Submediterranean Province of ammonites of the Mesogean affinity – such as Crussoliceras , G arnierisphinctes and Progeronia , as discussed above. Unit B in the Małogoszcz section has clearly the regressive character as indicated by its lithological characteristics (see above). The assemblage of ammonites consists mostly of Ataxioceratidae ( Crussoliceras , Garnierisphinctes and Progeronia ) and to lesser degree of the heavily-ribbed Aulacostephanidae ( Eurasenia , Prorasenia , rare Rasenia ), showing thus a marked similarity to that of unit A, but without Ataxioceras. The younger ammonite assemblage of unit C reveals, however, a markedly different character. The most important new faunal elements in ammonite assemblage of unit C are the suddenly appearing fairly numerous Aspidoceratidae, especially those of the genus Pseudhimalayites with the species P. uhlandi (Oppel). The roots of the genus were possibly in the Western Tethyan areas, or even far outside, thus a wide distribution of this genus in many European sections was an effect of migration (see e.g., Schweigert, 1997 ). The species P. uhlandi associated with many other Tethyan ammonites, such as various species of Nebrodites , occurs commonly in the Western Tethyan areas, and their foreland – in the Submediterranean Province, defining everywhere the upper part of the Divisum Zone or of the Herbichi Zone – the Uhlandi Subzone (e.g., Geyer, 1961 , Sarti, 1993 ; Caracuel et al., 1998 ). Even in the studied Submediterranean succession at Małogoszcz – some representatives of various species of Nebrodites have been encountered along with P. uhlandi in unit C. Additionally, the not numerous Aulacostephanidae are markedly impoverished here, both in number and in presence of heavily-ribbed forms. All these data strongly suggests a transgressive character of unit C. It should be remembered that the deposits of the Uhlandi Subzone are treated as transgressive in character in many areas of Europe (e.g., Marques & Olóriz, 1992 ). This high sea-level can be correlated possibly with the minimum of 100-kyr eccentricity cycle (see Boulila et al., 2008 , 2010 ). Units D and E in the Małogoszcz section yielded numerous specimens of Pseudhimalayites uhlandi (Oppel). Unfortunately the distribution of these specimens in the succession cannot be traced in details mostly because of lack of precise location of the particular finds. It is only the topmost part of unit E recognized which shows a marked concentration of the Pseudhimalayites shells, some of them attaining large sizes. In a similar stratigraphical position has been found also a few specimens of Phylloceratidae of giant sizes (about 0.5 m in diameter), interpreted herein as the allochtonous elements which appearance has been possibly related to the post-mortem drift of shells from the Tethyan areas (thus not taken into account in the diagram of distribution of the ammonite genera in the succession – see Fig. 2 ). It seems highly probable that the concentration of all these shells at the top of unit E resulted from a very high sea-level. This may correspond to the minimum of the next 100-kyr eccentricity cycle well documented in the late Divisum Subchron (see Boulila et al., 2008 , 2010 ). This level corresponds possibly also to the balderum horizon (or subzone) as marked by common occurrence of the Tethyan form Idoceras balderum (Oppel) well documented at the top of the Uhlandi Subzone of the Divisum Zone in the Submediterranean areas of southern Germany to south-eastern France (see e.g., Hantzpergue et al., 1997 ). Such stratigraphical interpretation can be also confirm by finding in the Małogoszcz section, at the top of unit E, of a single specimen of Taramelliceras ( Taramelliceras ) compsum (Oppel) of the Tethyan origin. Some changes in ammonites of the family Ataxioceratidae seen already in unit C, recognized also in units D-E include the emerging of the new genus Tolvericeras. The genus as interpreted by Enay et al. ( 2014 ) derived possibly from Garnierisphinctes and Crussoliceras. The rare specimens discovered in the Małogoszcz succession show a marked similarity to “ Tolvericeras n. sp.” in Gygi ( 2003 , p. 144, Figs. 165–166) coming from the Divisum Zone of northern Switzerland, showing independently some similarity to Garnierisphinctes. On the other hand, the units C-D-E yielded also numerous specimens of Crussoliceras [ C. cf. crusoliense (Font.)], Garnierisphinctes [ G. plebejus (Neumayr and G. championneti (Neum., G. semigarnieri (Geyer] and less common Progeronia [ P. ( P. ) eggeri (von Ammon), P. ( H. ) breviceps (Quenstedt)]. The recognized changes within family Aulacostephanidae in units D-E of the Małogoszcz section include especially the rare occurrences of the advanced morphologically representatives of the genus Rasenioides , such as R. moeschi (Oppel). Their appearance, already at the base of unit D, can be treated as a manifestation of “southern drift” of the genus which developed earlier in the Subboreal Province (see Wierzbowski, 2022 ; see also comments above): this phenomenon resulted possibly from appearance in the succession studied of marly facies resembling the “Virgulian Facies” of north-western Europe suitable for development of the Subboreal fauna (cf. Hantzpergue, 1995 ). On the other hand, the local occurrence of a special group of aulacostephanids intermediate between some Eurasenia and Pararasenia has been recognized in upper parts of unit E. They show heavy ornamentation on the whorl side characteristic of both Eurasenia and Pararasenia , but reveal an incipient obliteration of ribbing in the ventral side of whorls typical of the genus Pararasenia. The specimen (Fig. 7 c-d) studied resembles the heavily ribbed species Pararasenia quenstedti Durand (cf. Ziegler, 1962 ) reported in younger beds of the earliest Late Kimmeridgian in the Małogoszcz section (Kutek, 1968 ). Two specimens coming from units B and D-E (Fig. 7 a-b) are representatives of NW European Subboreal genus Rasenia. They show a weakly involute to weakly evolute coiling, rather distant primary ribs, and a high number of secondary ribs (the secondary/primary rib ratio equals 5.0 at about 50 mm diameter). The specimens belong to Rasenia involuta Spath, a very characteristic species commonly encountered in southern England where the specimens coming from (e.g., Birkelund et al., 1983 , Fig. 3 A-D) are very similar to the specimens studied. It is worth noting that all these specimens resemble also the heavily-ribbed form referred to as Rasenioides ecolisnus (Hantzpergue, 1989 , pl. 35: c-f). It should be remembered that the latter is treated as a form which begins a side branch of the Rasenioides lineage, leading in its evolutionary development to origin of a more heavily-ribbed forms of the genus Aulacostephanoides (Hantzpergue, 1989 , Figs. 130,133), or marking the transition to the genus Aulacostephanus (Borreli, 2014 , Fig. 2 ). The possible phylogenetical link between late Rasenia involuta , and some early forms of Aulacostephanoides/Aulacostephanus (as suggested herein) can be thus considered as an alternative proposal for the lineage (assuming the phylogenetical affinity between R. involuta and R. ecolisnus ), which developed independently of that leading from the densely-ribbed Rasenioides to the typical Aulacostephanoides (cf. Borreli, 2014 ). General comments The late Early Kimmeridgian corresponding to the late Hypselocyclum and Divisum chrons (or to the late Cymodoce Chron) was a fairly short time (about 260 to 300 kyr) when the diversity in development of many ammonites lineages changed markedly. This phylogenetical turnover resulted in origination and termination of several lineages, and has been strictly controlled by changes in the environment, generally in progress of the overall transgression, which occurred especially along the northern Tethyan Shelf in the wide areas of Submediterranean to Subboreal provinces of Europe. The transgression was strictly controlled by syn-sedimentary tectonic activity, and additionally superimposed transgressive pulses corresponding to climate changes, related mostly with orbitally-controlled cyclicity. The studied Submediterranean succession at Małogoszcz in the south-western margin of the Holy Cross Mountains, central Poland was formed in changing water depth – from initial transgression flooding the shallow-water carbonate platform to a fairly deep water environment, which showed similarity to that of the “Virgulian Facies” of north-western Europe. The development of the coeval deeper-water sedimentation is recognized widely in Submediterranean areas from central Poland to south-eastern France and Spain, being everywhere strictly correlated to the marked evolutionary transformations of the ammonite faunas: their migrations, decline or radiation. The beginning of the marine transgression already at the end of the Hypselocyclum Chron brought into the whole discussed areas of Submediterranean Europe the new ataxioceratid ammonites including closely related genera Crussoliceras , Garnierisphinctes and Progeronia having possibly their roots in the Mediterranean Tethys. The development of these ammonites was strictly related to changes of the environmental conditions into those compatible with their physiological tolerance, which also affected the group of older indigenous Ataxioceratinae, such as Ataxioceras , Orthosphinctes and Ardescia , and resulted in its total decline. On the other hand, the changes in environment strongly disturbed also the development of other groups of ammonites, mostly Aulacostephanidae: some of them, especially the heavily- ribbed forms ( Eurasenia , Involuticeras ) fluorished on the flooded areas of the carbonate platform like that of the Holy Cross Mts., some other like the more open-marine Rasenioides migrated toward the north into a deeper-water environment of Subboreal Province. The progress of the transgression brought onto the Tethyan Shelf (but also into the Mediterranean Tethys) during the late Divisum Chron also other ammonites – mostly Aspidoceratidae, especially of the genus Pseudhimalayites. The taxonomic diversity within Crussoliceras-Garnierisphinctes-Progeronia faunas increases upwards in the succession studied at Małogoszcz. This is shown by the appearance of larger number of species, but also by the evolutionary development of the new genus Tolvericeras showing affinity to Garnierisphinctes. It is in general accordance with observation of Enay et al. ( 2014 ) who suggested the evolutionary path from Garnierisphinctes to restricted group of species placed around the type species of Tolvericeras already during the late Divisum Chron, at the end of Early Kimmeridgian, in the Submediterranean Province in SE France and Switzerland. Later on, Crussoliceras and Tolvericeras were rather not commonly encountered here, occurring mostly during the Late Kimmeridgian in the Western European Swell – the transitional area between Submediterranean and Subboreal provinces, where also some forms close to Crussoliceras evolved at the end of the Kimmeridgian into Pseudogravesia to Gravesia group (Enay et al., 2014 ; cf. also Hantzpergue et al., 1989). On the other hand, a more common occurrence of Crussoliceras and Tolvericeras during the Late Kimmeridgian has been recognized in the Subboreal Province in England: the appearance there of Subdichotomites , which possibly evolved from Crussoliceras at the end of the Kimmeridgian, gave subsequently rise to the Boreal Dorsoplanitinae (Enay et al., 2014 ). The evolutionary development of Aulacostephanidae at the end of the Early Kimmeridgian – beginning of the Late Kimmeridgian in Europe has been the subject of fairly diversified interpretations. This is mostly because of the incompleteness of the fossil records, at least partly resulting from marked changes of palaeobiogeographical ranges of these ammonites in time. The only indigenous lineage traced in the Holy Cross Mts. area is that leading from the heavily-ribbed Eurasenia , like E. pendula and E. trifurcata recorded in the succession studied, to Pararasenia which shows the smooth band in the ventral side of whorls (Ziegler, 1962 ; see also Wierzbowski, 2022 ). Another lineage, already discussed above, originated from the weakly-ornamented Vineta to Rasenioides , but its further development included migration of younger forms of the lineage towards the north where they gave rise to early Aulacostephanoides. Even more nebulous is the development of the third lineage of aulacostephanids. This possibly included at its base some moderately involute and heavily-ribbed Rasenia (like R. involuta and possibly similarly looking “ Rasenioides ” ecolisnus , as discussed above). They seem to intergrade even with the “transitional” genus Zonovia showing some weakening of the ribbing on the ventral side of outer whorls (see Birkelund et al., 1978 ). The lineage may continue into some more heavily-ribbed early Late Kimmeridgian aulacostephanids referred in older classifications to as Aulacostephanoides , and more recently correlated with Aulacostephanus (Borreli, 2014 ). The changes in distribution of ammonites were accompanied by important development in their evolution. Such a drastic example of overlapping of ranges of distribution of the ammonite faunas belonging to different lineages and representing the various stages of their evolutionary development has been reported in the successions of central and southern parts of the Russian Platform, especially Tatarstan, central European Russia (see Rogov et al., 2017 ). The recognized there a narrow stratigraphical horizon with Submediterranean Crussoliceras atavum (Schneid) - C. lacertosum (Fonatnnes), possibly corresponds only to some upper parts of the Divisum Zone, and it is underlain by beds with Subboreal Rasenia and Zonovia , and overlain by beds with Rasenioides , all of them belonging to the upper part of the Cymodoce Zone – the Askepta Subzone. Additionally, the occasional occurrence of the Boreal ammonites of the genus Amoebites , transitional already to younger Euprionoceras , indicates the evolutionary changes in the cardioceratid lineage during the late Kitchini Chron. The problems of general classification of the Late Kimmeridgian ammonites attributed to the genus Aulacostephanus is generally outside the scope of the present study. It is only the genus Zenostephanus (formerly Xenostephanus ) which evolutionary development is partly related to those of some discussed here aulacostephanids, and which represents a similar stratigraphical range. The genus evolved probably from the Subboreal Rasenia evoluta , as evidenced by occurrence of the intermediate forms already at the end of the Cymodoce Chron in southern England (Birkelund et al., 1983 ). These migrated successively into the Arctic areas of the Boreal Province at the boundary between the Early and Late Kimmeridgian as a consequence of a large transgression giving then the onset to the new lineage (e.g., Wierzbowski & Smelror, 2020 ), but appeared soon thereafter as representatives of the fully developed genus Zenostephanus in north-eastern Europe in areas of the Russian Sea (Rogov et al., 2017 ). 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Monographie der Perisphinctidae des unteren Unterkimeridgium (Weisser Jura ɣ, Badenerschichten) im sȕddeutschen Jura. Palaeontographica , 117A (1–4), 1–157. Gygi, R. (2003). Perisphinctacean ammonites of the late Jurassic in northern Switzerland: a versatile tool to investigate the sedimentary geology of an epicontinental sea. Schweizerische Paläontologische Abhandlungen , 123 , 1–232. Gygi, R., & Persoz, F. (1986). Mineralogy, litho- and biostratigraphy combined in correlation of the Oxfordian (late Jurassic) formations of the Swiss Jura range. Eclogae Geologicae Helvetiae , 79 (2), 385–454. Hantzpergue, P. (1989). Les ammonites kimmeridgiénnes du haut-fond d’Europe occidentale: biochronologie, systématique, evolution, paléobiogéographie (pp. 1–425). Centre National de la Recherche Scientifique. Paris. Hantzpergue, P. (1995). Faunal trends and sea-level changes: biostratigraphic patterns of Kimmeridgian ammonites on the Western European Shelf. Geologische Rundschau , 84 , 245–254. Hantzpergue, P., Atrops, F., & Enay, R. (1997). Kimméridgien. In E.Cariou & P. Hantzpergue (Coord.): Biostratigraphie du Jurassique oust-européen et méditerranéen. Bulletin Centre de Recherches Elf Exploration-Production, 17 , 87–96. Jank, M., Meyer, C. A., & Wetzel, A. (2006). Late Oxfordian to Late Kimmeridgian carbonate deposits of NW Switzerland (Swiss Jura): stratigraphical and palaeogeographical implications in the transition area between the Paris Basin and the Tethys. Sedimentary Geology , 186 , 237–263. Kaźmierczak, J., & Pszczółkowski, A. (1968). Sedimentary discontinuities in the Lower Kimmeridgian of the Holy Cross Mts. Acta Geologica Polonica , 18 (3), 587–612. Książkiewicz, M., & Samsonowicz, J. (1953). Zarys geologii Polski. Państwowe Wydawnictwa Naukowe. Warszawa. Kutek, J. (1968). The Kimmeridgian and uppermost Oxfordian in the SW margin of the Holy Cross Mts. (Central Poland). Part I. Stratigraphy. Acta Geologica Polonica , 18 (3), 494–586. (in Polish with English summary). Kutek, J. (1994). Jurassic tectonic events in south-eastern cratonic Poland. Acta Geologica Polonica , 44 (3–4), 167–221. Kutek, J., & Głazek, J. (1972). The Holy Cross area, central Poland in the Alpine cycle. Acta Geologica Polonica , 22 (4), 603–652. Machalski, M. (1993). Ławice ostrygowe kimerydu obrzeżenia Gór Świętokrzyskich. Unpublished Ph.D Thesis (pp. 1-215), Institute of Paleobiology, Polish Academy of Sciences. Marques, B., & Olóriz, F. (1992). The Orthaspidoceras uhlandi (Oppel) record and the maximum flooding in the eastern Algarve during the Lower Kimmeridgian. Revista Española de Paleontologia, 1992 , 149–156. Matyja, B. A. (2011). Płytkowodna platforma węglanowa późnej jury na południowo-zachodnim obrzeżeniu Gór Świętokrzyskich. In B. A. Matyja, A. Wierzbowski, & P. Ziółkowski (Eds.), Jurassica IX, Małogoszcz, 06–08 września 2011, Materiały konferencyjne (pp. 133–151). Polskie Towarzystwo Geologiczne. Matyja, B. A., & Wierzbowski, A. (2000). Biostratigraphical correlations between the Subboreal Mutabilis Zone and the Submediterranean upper Hypselocyclum – Divisum zones of the Kimmeridgian: new data from northern Poland. GeoResearch Forum , 6 , 129–136. Matyja, B. A., Wierzbowski, A., Radwańska, U., & Radwański, A. (2006). Małogoszcz, large quarry of cement works (Lower and lowermost Upper Kimmeridgian). In A. Wierzbowski, et al. (Eds.), Jurassic of Poland and adjacent Slovakian Carpathians, Field trip guidebook of 7th International Congress on the Jurassic System (pp. 190–198). Polish Geological Institute. Moliner, L. (2009). Ataxioceratinae (Ammonitina) del Kimmeridgiense inferior en el NE de la Provincia de Terueal (Cordillera Ibérica Oriental y Maestrazgo). Tesis Doctoral (pp.1-533), Departamento de Estratigrafia y Paleontologia, Universidad de Granada. Moliner, L., & Olóriz, F. (2009). Updated biostratigraphy of Jurassic (lower Kimmeridgian) deposits containing the ammonite Ataxioceras from the eastern Iberian Range, northeastern Spain. GFF , 131 , 193–203. Moliner, L., & Olóriz, F. (2010). New Lower Kimmeridgian ataxioceratin ammonite from the eastern Iberian Chain, Spain: Systematic, biogeographic, and biostratigraphic relevance. Acta Palaeontologica Polonica , 55 (1), 99–110. Olóriz, F. (1978). Kimmeridgiense-Tithonico inferior en el sector central de las Cordilleras Beticas (Zona Subbetica). Paleontologia. Biostratigrafia. Tesis Doctorales de la Universidad de Granada, 184 , tomo I (pp 1-758), tomo 2 (atlas). Pavia, G., Benetti, A., & Minetti, C. (1987). Il Rosso Ammonitico dei Monti Lessini Veronesi (Italia NE). Fauna ad ammoniti e discontinuità stratigrafische nel Kimmeridgiano inferiore. Bolletino della Società Paleontologica Italiana , 26 (1–2), 63–92. Rogov, M. A., Wierzbowski, A., & Shchepetova, E. (2017). Ammonite assemblages in the Lower to Upper Kimmeridgian boundary interval (Cymodoce to Mutabilis zones) of Tatarstan (central European Russia) and their correlation importance. Neues Jahrbuch fȕr Geologie und Paläontologie,285 , (2), 161–185. 10.1127/njgpa/2017/0675 . Sarti, C. (1993). Il Kimmeridgiano delle Prealpi Veneto-Trentine: fauna e biostratigrafia. Memoire del Museo di Storia Naturale di Verona (II serie), Sezione Scienze della Terra, 5 , 1-145. Sapunov, I. G. (1979). Les Fossiles de Bulgarie. III.3. Jurassique supérieur. Ammonoidea (pp. 1-237). Academie Bulgare des Sciences. Sofia, 1979. Schweigert, G. (1997). Die Ammonitengattungen Simocosmoceras Spath and Pseudhimalayites Spath (Aspidoceratidae) im sȕddeutschen Oberjura. Stuttgarter Beiträge zur Naturkunde Serie B (Geologie und Paläontologie) , 246 , 1–29. Schweigert, G., & Kuschel, H. (2017). Comments on the identification of Ammonites planula Hehl in Zieten, 1830 (Upper Jurassic, SW Germany). Volumina Jurassica , 15 , 1–16. 10.5604/01.3001.0010.3920 . Seilacher, U., Matyja, B. A., & Wierzbowski, A. (1985). Oyster beds – morphologic response to changing substrate conditions. In U. Bayer, & A. Seilacher (Eds.), Sedimentary and evolutionary cycles. Lecture Notes in Earth Sciences, 1 (pp. 421–435). Springer. Wierzbowski, A. (2017). The Lower Kimmeridgian of the Wieluń Upland and adjoining regions in central Poland: lithostratigraphy, ammonite stratigraphy (upper Planula/Platynota to Divisum zones), palaeogeography and climate-controlled cycles. Volumina Jurassica , 15 , 41–120. 10.5604/01.3001.0010.5659) . Wierzbowski, A. (2020). The Kimmeridgian of the south-western margin of the Holy Cross Mts., central Poland: stratigraphy and facies development. Part 1. From deep-neritic sponge megafacies to shallow water carbonates. Volumina Jurassica , 18 (2), 161–234. 10.7306/VJ.18.8) . Wierzbowski, A. (2022). Phylogeny of the ammonite family Aulacostephanidae Spath, 1924 during the Late Oxfordian and the Early Kimmeridgian in Europe: main lineages, patterns of evolution, and sedimentological to palaeogeographical controls on evolutionary development. Volumina Jurassica , 20 , 59–128. 10.7306/VJ.20.3) . Wierzbowski, A., & Smelror, M. (2020). The Bajocian to Kimmeridgian (Middle to Upper Jurassic) ammonite succession at Sentralbanken High (core 7533/3-U-1), Barents Sea, and its stratigraphical and palaeogeographical significance. Volumina Jurassica , 18 (1), 1–22. 10.7306/VJ.18.1) . Wierzbowski, A., Smoleń, J., & Iwańczuk, J. (2015). The Oxfordian and Lower Kimmeridgian of the Peri-Baltic Syneclise (north-eastern Poland: stratigraphy, ammonites, microfossils (foraminifers, radiolarians), facies and palaeogeographical implications. Neues Jahrbuch fȕr Geologie und Paläontologie , 277 (1), 63–104. 10.1127/njgpa/2015/0496) . Wierzbowski, H. (2019). Palaeoenvironmental changes recorded in oxygen and carbon isotope composition of Kimmeridgian (Upper Jurassic) carbonates from central Poland. Geological Quarterly , 63 (2), 259–274. http://dx.doi.org/10.7306/gq.1471) . Ziegler, B. (1979). Idoceras und verwandte Ammoniten_Gattungen im Oberjura Schwabens. Eclogae Geologicae Helvetiae , 52 (1), 19–56. Ziegler, B. (1962). Die Ammoniten Gattung Aulacostephanus im Oberjura (Taxonomie, Stratigraphie, Biologie). Palaeontographica , 119A , 1–172. Cite Share Download PDF Status: Published Journal Publication published 26 Sep, 2024 Read the published version in Journal of Iberian Geology → Version 1 posted Reviewers agreed at journal 30 Apr, 2024 Reviewers invited by journal 16 Apr, 2024 Editor invited by journal 13 Mar, 2024 Editor assigned by journal 12 Mar, 2024 First submitted to journal 12 Mar, 2024 You are reading this latest preprint version Research Square lets you share your work early, gain feedback from the community, and start making changes to your manuscript prior to peer review in a journal. As a division of Research Square Company, we’re committed to making research communication faster, fairer, and more useful. We do this by developing innovative software and high quality services for the global research community. Our growing team is made up of researchers and industry professionals working together to solve the most critical problems facing scientific publishing. Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {\"props\":{\"pageProps\":{\"initialData\":{\"identity\":\"rs-4008521\",\"acceptedTermsAndConditions\":true,\"allowDirectSubmit\":false,\"archivedVersions\":[],\"articleType\":\"Research Article\",\"associatedPublications\":[],\"authors\":[{\"id\":291986510,\"identity\":\"073e40aa-2375-4e38-b673-63dabc63869b\",\"order_by\":0,\"name\":\"Andrzej Wierzbowski\",\"email\":\"data:image/png;base64,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\",\"orcid\":\"\",\"institution\":\"University of Warsaw, Faculty of Geology\",\"correspondingAuthor\":true,\"prefix\":\"\",\"firstName\":\"Andrzej\",\"middleName\":\"\",\"lastName\":\"Wierzbowski\",\"suffix\":\"\"}],\"badges\":[],\"createdAt\":\"2024-03-03 12:12:53\",\"currentVersionCode\":1,\"declarations\":\"\",\"doi\":\"10.21203/rs.3.rs-4008521/v1\",\"doiUrl\":\"https://doi.org/10.21203/rs.3.rs-4008521/v1\",\"draftVersion\":[],\"editorialEvents\":[{\"content\":\"https://doi.org/10.1007/s41513-024-00260-y\",\"type\":\"published\",\"date\":\"2024-09-26T15:58:00+00:00\"}],\"editorialNote\":\"\",\"failedWorkflow\":false,\"files\":[{\"id\":54975165,\"identity\":\"1a928ec2-1ede-4cd2-a472-b25e636a97e1\",\"added_by\":\"auto\",\"created_at\":\"2024-04-19 12:37:57\",\"extension\":\"png\",\"order_by\":1,\"title\":\"Figure 1\",\"display\":\"\",\"copyAsset\":false,\"role\":\"figure\",\"size\":201824,\"visible\":true,\"origin\":\"\",\"legend\":\"\\u003cp\\u003eGeological map of the Holy Cross Mountains (after Samsonowicz in Książkiewicz \\u0026amp; Samsonowicz, 1953, somewhat modified) showing the position of the Małogoszcz cement-work quarry section.\\u003c/p\\u003e\",\"description\":\"\",\"filename\":\"1.png\",\"url\":\"https://assets-eu.researchsquare.com/files/rs-4008521/v1/489100543c27db5e52883d69.png\"},{\"id\":54974874,\"identity\":\"183eb8d1-b1a4-41a1-bda8-1ee8f86c363f\",\"added_by\":\"auto\",\"created_at\":\"2024-04-19 12:29:57\",\"extension\":\"png\",\"order_by\":2,\"title\":\"Figure 2\",\"display\":\"\",\"copyAsset\":false,\"role\":\"figure\",\"size\":77439,\"visible\":true,\"origin\":\"\",\"legend\":\"\\u003cp\\u003eGeological section of the discussed deposits of the uppermost Lower Kimmeridgian in the Małogoszcz section (after Matyja et al., 2006) showing position of the distinguished lithological units A-E, their chronostratigraphical interpretation, and changing patterns of ammonite distribution at the family level in the succession.\\u003c/p\\u003e\",\"description\":\"\",\"filename\":\"FIG.2.png\",\"url\":\"https://assets-eu.researchsquare.com/files/rs-4008521/v1/aca81465c280ead5441d8c21.png\"},{\"id\":54974872,\"identity\":\"54b169a2-c03b-4751-90fd-e4430dc8f39d\",\"added_by\":\"auto\",\"created_at\":\"2024-04-19 12:29:57\",\"extension\":\"jpg\",\"order_by\":3,\"title\":\"Figure 3\",\"display\":\"\",\"copyAsset\":false,\"role\":\"figure\",\"size\":1817161,\"visible\":true,\"origin\":\"\",\"legend\":\"\\u003cp\\u003eAmmonites \\u003cem\\u003eAtaxioceras \\u003c/em\\u003eand \\u003cem\\u003eGarnierisphinctes \\u003c/em\\u003e\\u0026nbsp;from the upper Hypselocyclum Zone (Lothari Subzone) to lower Divisum Zone (Crusoliensis Subzone).\\u003c/p\\u003e\\n\\u003cp\\u003ea – \\u003cem\\u003eAtaxioceras \\u003c/em\\u003e(\\u003cem\\u003eParataxioceras\\u003c/em\\u003e) \\u003cem\\u003eoppeli parvum \\u003c/em\\u003eAtrops, microconch; ZI/100/41; unit A.\\u003c/p\\u003e\\n\\u003cp\\u003eb – \\u003cem\\u003eAtaxioceras \\u003c/em\\u003e(\\u003cem\\u003eParataxioceras\\u003c/em\\u003e) cf. \\u003cem\\u003eplanulatum \\u003c/em\\u003e(Quenstedt); microconch; ZI/100/42; unit A.\\u003c/p\\u003e\\n\\u003cp\\u003ec – “\\u003cem\\u003eOrthosphinctes \\u003c/em\\u003e(\\u003cem\\u003eArdescia\\u003c/em\\u003e)” \\u003cem\\u003eperayensis \\u003c/em\\u003eAtrops, microconch; ZI/100/44; unit A.\\u003c/p\\u003e\\n\\u003cp\\u003ed – \\u003cem\\u003eGarnierisphinctes melliconense \\u003c/em\\u003e(Geyer), ? microconch; ZI/100/45; unit A.\\u003c/p\\u003e\\n\\u003cp\\u003ee – \\u003cem\\u003eGarnierisphinctes \\u003c/em\\u003ecf. \\u003cem\\u003egarnieri \\u003c/em\\u003e(Fontannes), ? microconch; ZI/100/85; unit B.\\u003c/p\\u003e\\n\\u003cp\\u003ePhragmocone/body chamber boundary is arrowed.\\u003c/p\\u003e\",\"description\":\"\",\"filename\":\"FIG.32.jpg\",\"url\":\"https://assets-eu.researchsquare.com/files/rs-4008521/v1/f0f76b000451ae508f17590d.jpg\"},{\"id\":54974876,\"identity\":\"45a623e0-51cb-41dc-bf15-3a5f52d94999\",\"added_by\":\"auto\",\"created_at\":\"2024-04-19 12:29:57\",\"extension\":\"jpg\",\"order_by\":4,\"title\":\"Figure 4\",\"display\":\"\",\"copyAsset\":false,\"role\":\"figure\",\"size\":1645191,\"visible\":true,\"origin\":\"\",\"legend\":\"\\u003cp\\u003eAmmonites \\u003cem\\u003eCrussoliceras \\u003c/em\\u003eand \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e from the upper Hypselocyclum Zone (Lothari Subzone) to lower Divisum Zone (Crusoliensis Subzone).\\u003c/p\\u003e\\n\\u003cp\\u003ea – \\u003cem\\u003eCrussoliceras sayni \\u003c/em\\u003e(Camus et Thieuloy), phragmocone, ? macroconch; ZI/10046; unit A.\\u003c/p\\u003e\\n\\u003cp\\u003eb – \\u003cem\\u003eGarnierisphinctes garnieri \\u003c/em\\u003e(Fontannes), microconch; ZI/100/56 (imprint from original specimen); unit A.\\u003c/p\\u003e\\n\\u003cp\\u003ec-d – \\u003cem\\u003eCrussoliceras \\u003c/em\\u003ecf. \\u003cem\\u003eaceroides \\u003c/em\\u003eGeyer; fragments of body-chamber with a part of phragmocone (B); ZI/100/87,88; unit B.\\u003c/p\\u003e\",\"description\":\"\",\"filename\":\"FIG.41.jpg\",\"url\":\"https://assets-eu.researchsquare.com/files/rs-4008521/v1/5a08c804bb4e4e5fb06b394c.jpg\"},{\"id\":54974879,\"identity\":\"ac3f6438-5a92-4b7f-97dd-5ec499e7f040\",\"added_by\":\"auto\",\"created_at\":\"2024-04-19 12:29:57\",\"extension\":\"jpg\",\"order_by\":5,\"title\":\"Figure 5\",\"display\":\"\",\"copyAsset\":false,\"role\":\"figure\",\"size\":1653986,\"visible\":true,\"origin\":\"\",\"legend\":\"\\u003cp\\u003eAmmonites \\u003cem\\u003eProgeronia\\u003c/em\\u003e from the upper part of the Hypselocyclum Zone (Lothari Subzone) and the upper part of the Divisum Zone (Uhlandi Subzone).\\u003c/p\\u003e\\n\\u003cp\\u003ea – \\u003cem\\u003eProgeronia \\u003c/em\\u003e(\\u003cem\\u003eProgeronia\\u003c/em\\u003e) \\u003cem\\u003eprogeron \\u003c/em\\u003e(von Ammon), macroconch; ZI/100/52; unit A.\\u003c/p\\u003e\\n\\u003cp\\u003eb – \\u003cem\\u003eProgeronia \\u003c/em\\u003e(\\u003cem\\u003eHugueninsphinctes\\u003c/em\\u003e) \\u003cem\\u003ebreviceps \\u003c/em\\u003e(Quenstedt), microconch; ZI/100/53; unit A.\\u003c/p\\u003e\\n\\u003cp\\u003ec - \\u003cem\\u003eProgeronia \\u003c/em\\u003e(\\u003cem\\u003eHugueninsphinctes\\u003c/em\\u003e) \\u003cem\\u003ebreviceps \\u003c/em\\u003e(Quenstedt), microconch; ZI/100/100; unit C.\\u003c/p\\u003e\\n\\u003cp\\u003ed – \\u003cem\\u003eProgeronia \\u003c/em\\u003e(\\u003cem\\u003eProgeronia\\u003c/em\\u003e) cf. \\u003cem\\u003eeggeri \\u003c/em\\u003e(von Ammon); ZI/100/120; units D-E.\\u003c/p\\u003e\\n\\u003cp\\u003ePhragmocone/body chamber boundary is arrowed.\\u003c/p\\u003e\",\"description\":\"\",\"filename\":\"FIG.51.jpg\",\"url\":\"https://assets-eu.researchsquare.com/files/rs-4008521/v1/c2e10f8d6beaaca8cba74b85.jpg\"},{\"id\":54975167,\"identity\":\"cb202594-a7a8-4927-94a6-99747ad2e2b1\",\"added_by\":\"auto\",\"created_at\":\"2024-04-19 12:37:57\",\"extension\":\"jpg\",\"order_by\":6,\"title\":\"Figure 6\",\"display\":\"\",\"copyAsset\":false,\"role\":\"figure\",\"size\":1571927,\"visible\":true,\"origin\":\"\",\"legend\":\"\\u003cp\\u003eAmmonites \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eTolvericeras \\u003c/em\\u003efrom the upper part of the Divisum Zone (Uhlandi Subzone).\\u003c/p\\u003e\\n\\u003cp\\u003ea – \\u003cem\\u003eGarnierisphinctes semigarnieri \\u003c/em\\u003e\\u0026nbsp;(Geyer), phragmocone with a part of the body-chamber; ZI/100/101; unit C.\\u003c/p\\u003e\\n\\u003cp\\u003eb - \\u003cem\\u003eGarnierisphinctes championneti \\u003c/em\\u003e(Fontannes), microconch; ZI/100/10; unit C.\\u003c/p\\u003e\\n\\u003cp\\u003ec – \\u003cem\\u003eGarnierisphinctes plebejus \\u003c/em\\u003e(Neumayr), phragmocone, imprints of fragmentary preserved ribs of the outer whorl belong possibly to the body-chamber; ZI/100/103; unit C.\\u003c/p\\u003e\\n\\u003cp\\u003ed - ? \\u003cem\\u003eTolvericeras \\u003c/em\\u003esp.; ZI/100/106; unit C.\\u003c/p\\u003e\\n\\u003cp\\u003ePhragmocone/body chamber boundary is arrowed.\\u003c/p\\u003e\",\"description\":\"\",\"filename\":\"FIG.61.jpg\",\"url\":\"https://assets-eu.researchsquare.com/files/rs-4008521/v1/fb5992a5fbcca9c768186e8f.jpg\"},{\"id\":54974877,\"identity\":\"ddddc330-b102-4b56-9969-ae2be8ded174\",\"added_by\":\"auto\",\"created_at\":\"2024-04-19 12:29:57\",\"extension\":\"jpg\",\"order_by\":7,\"title\":\"Figure 7\",\"display\":\"\",\"copyAsset\":false,\"role\":\"figure\",\"size\":2181462,\"visible\":true,\"origin\":\"\",\"legend\":\"\\u003cp\\u003eAmmonites of the families Aulacostephanidae, \\u0026nbsp;Perisphinctidae and Oppeliidae from the upper part of the Hypselocyclum Zone (Lothari Subzone) and the Divisum Zone\\u003c/p\\u003e\\n\\u003cp\\u003ea – \\u003cem\\u003eRasenia involuta \\u003c/em\\u003eSpath; macroconch; ZI/100/74; unit B.\\u003c/p\\u003e\\n\\u003cp\\u003eb - \\u003cem\\u003eRasenia involuta \\u003c/em\\u003eSpath; macroconch; ZI/100/116; unit D-E.\\u003c/p\\u003e\\n\\u003cp\\u003ec-d - ? \\u003cem\\u003ePararasenia \\u003c/em\\u003eaff. \\u003cem\\u003equenstedti \\u003c/em\\u003e(Durand), macroconch, phragmocone, lateral (A) and ventral (B) views; ZI/100/118, units D-E.\\u003c/p\\u003e\\n\\u003cp\\u003ee – \\u003cem\\u003eNebrodites maccerimus \\u003c/em\\u003e(Quenstedt), microconch; ZI/100/51; unit A.\\u003c/p\\u003e\\n\\u003cp\\u003ef – \\u003cem\\u003eNebrodites favaraensis \\u003c/em\\u003e(Gemmellaro), body chamber; ZI/100/98; unit C.\\u003c/p\\u003e\\n\\u003cp\\u003eg-h-i – \\u003cem\\u003ePresimoceras \\u003c/em\\u003eex gr. \\u003cem\\u003eP. herbichi \\u003c/em\\u003e(? \\u003cem\\u003eP.nodulatum \\u003c/em\\u003e(Quenstedt); body chamber, lateral (A and B) and ventral view (C); ZI/100/82,83; unit B.\\u003c/p\\u003e\\n\\u003cp\\u003ej – \\u003cem\\u003eNebrodites \\u003c/em\\u003ecf. \\u003cem\\u003eagrigentinus \\u003c/em\\u003e(Gemmellaro), phragmocone with a part of the body-chamber; ZI/100/99, unit C.\\u003c/p\\u003e\\n\\u003cp\\u003ek – \\u003cem\\u003eIdoceras balderum \\u003c/em\\u003e(Oppel); outer whorl is a body chamber; ZI/100/81 (imprint from original specimen); unit B.\\u003c/p\\u003e\\n\\u003cp\\u003el – \\u003cem\\u003eTaramelliceras \\u003c/em\\u003e(\\u003cem\\u003eTaramelliceras\\u003c/em\\u003e) \\u003cem\\u003ecompsum \\u003c/em\\u003e(Oppel), phragmocone; ZI/100/111; units D-E (?E).\\u003c/p\\u003e\\n\\u003cp\\u003ePhragmocone/body chamber boundary is arrowed.\\u003c/p\\u003e\",\"description\":\"\",\"filename\":\"FIG.7.jpg\",\"url\":\"https://assets-eu.researchsquare.com/files/rs-4008521/v1/6c186cdf612b191263642b9b.jpg\"},{\"id\":54975166,\"identity\":\"8ddbaa6a-ebc6-4c99-880a-3a47fe3d4bd2\",\"added_by\":\"auto\",\"created_at\":\"2024-04-19 12:37:57\",\"extension\":\"png\",\"order_by\":8,\"title\":\"Figure 8\",\"display\":\"\",\"copyAsset\":false,\"role\":\"figure\",\"size\":68395,\"visible\":true,\"origin\":\"\",\"legend\":\"\\u003cp\\u003ePhylogenetical development and palaeobiogeographical affinity of ammonites from the uppermost Lower Kimmeridgian of the Małogoszcz section.\\u003c/p\\u003e\",\"description\":\"\",\"filename\":\"FIG.8.png\",\"url\":\"https://assets-eu.researchsquare.com/files/rs-4008521/v1/cdabf25b1a38d28f3bbce085.png\"},{\"id\":65628681,\"identity\":\"ceeb061f-7956-4fab-a15b-5eac7ee57fee\",\"added_by\":\"auto\",\"created_at\":\"2024-09-30 16:19:23\",\"extension\":\"pdf\",\"order_by\":0,\"title\":\"\",\"display\":\"\",\"copyAsset\":false,\"role\":\"manuscript-pdf\",\"size\":35089704,\"visible\":true,\"origin\":\"\",\"legend\":\"\",\"description\":\"\",\"filename\":\"manuscript.pdf\",\"url\":\"https://assets-eu.researchsquare.com/files/rs-4008521/v1/030257a7-e5b8-4068-aa85-5048511c3aab.pdf\"}],\"financialInterests\":\"\",\"formattedTitle\":\"The ammonite faunas of the upper Hypselocyclum to Divisum zones (Lower Kimmeridgian, Upper Jurassic) at Małogoszcz, Holy Cross Mts., central Poland: their stratigraphical interpretation and evolutionary development\",\"fulltext\":[{\"header\":\"Introduction\",\"content\":\"\\u003cp\\u003e \\u003cem\\u003eGeological setting\\u003c/em\\u003e. The Upper Jurassic deposits occurring around the Paleozoic core of the Holy Cross Mountains (Polish: Świętokrzyskie Mountains) in central Poland, in the north-eastern, the north-western and the south-western margins, represent remnants of the primary cover developed originally over the whole area. The lateral extent of the Upper Jurassic deposits was modified by Neo-Cimmerian (pre-Albian) tectonic movements and markedly changed by Laramian (at the end of Maastrichtian and during Palaeocene) uplift of the mountains which became the south-eastern fragment of the elevated zone of the Middle Polish Anticlinorium (Kutek \\u0026amp; Głazek, \\u003cspan citationid=\\\"CR29\\\" class=\\\"CitationRef\\\"\\u003e1972\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eThe Upper Jurassic deposits are accessible for detailed study in several large quarries, including that of the Małogoszcz cement works in the south-western margin of the mountains (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig1\\\" class=\\\"InternalRef\\\"\\u003e1\\u003c/span\\u003e), where the detailed Kimmeridgian succession of carbonates has been described from (Matyja et al., \\u003cspan citationid=\\\"CR34\\\" class=\\\"CitationRef\\\"\\u003e2006\\u003c/span\\u003e). The stratigraphical succession studied here, attaining about 25 meters in thickness, corresponds to the Skork\\u0026oacute;w Lumachelle of Kutek (\\u003cspan citationid=\\\"CR27\\\" class=\\\"CitationRef\\\"\\u003e1968\\u003c/span\\u003e). It consists of oyster lumachelles, micritic limestones and marls rich in various fossils and oncoids representing the transgressive part of sedimentary sequence, covering the older shallow-water marls and sublithographic limestones deposited in restricted environment with a very poor fauna. The latter represent the final regressive fragment of an older sequence developed at the decline of the shallow-water carbonate platform (e.g., Kutek, \\u003cspan citationid=\\\"CR28\\\" class=\\\"CitationRef\\\"\\u003e1994\\u003c/span\\u003e). A substantial fossil assemblage listed by Radwańska \\u0026amp; Radwański (in: Matyja et al., \\u003cspan citationid=\\\"CR34\\\" class=\\\"CitationRef\\\"\\u003e2006\\u003c/span\\u003e) comprises numerous bivalves (both deep infaunal to epifaunal oysters \\u0026ndash; such as \\u003cem\\u003eActinostreon\\u003c/em\\u003e and \\u003cem\\u003eNanogyra \\u0026ndash;\\u003c/em\\u003e forming mass accumulations), ammonites, brachiopods, lobsters, regular and irregular echinoids, starfish, crinoids and various fish remains, some of them bored by bryozoans and bivalves and/or encrusted by diverse epizoans such as serpulids and bryozoans.\\u003c/p\\u003e \\u003cp\\u003e \\u003cem\\u003eMaterials and methodology\\u003c/em\\u003e. The ammonites occur fairly commonly. The collection of ammonites consisting of over 200 specimens determined to the genus level (and additionally in a large part to the species level) is composed of common representatives of three families: Ataxioceratidae, Aulacostephanidae and Aspidoceratidae, and rare ones of two others: Perisphinctidae and Oppeliidae. These ammonites have been picked during several years personally and donated by other persons during occasional visit in the quarry, being usually referred to the particular lithostratigraphical units (also after study of the matrix), but commonly without precise location therein. The most valuable specimens of the collection are housed in the Museum of the Geological Faculty of the University of Warsaw (collection number ZI/100).\\u003c/p\\u003e \\u003cp\\u003eThe dimorphism of ammonites, if strongly marked in shell morphology, is expressed morphotaxonomically both at the generic and species levels. This refers especially to the most commonly recognized forms of the families Ataxioceratidae and Aulacostephanidae whose taxonomical interpretation accepted herein is especially close to those presented by Atrops (\\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e) in relation to Ataxioceratidae, and by Wierzbowski (\\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e) in relation to Aulacostephanidae. Such an approach, although purely descriptive is \\u0026ldquo;fully conscious\\u0026rdquo;, because it makes easier study of evolutionary transformations in the lineages, especially those constraint by heterochrony, closely related to changes in environmental conditions.\\u003c/p\\u003e \\u003cp\\u003eThe whole succession studied can be subdivided into five units differing in lithology which along with stated differences in composition and preservation of faunal assemblages make possible recognition of the changes in the environmental conditions. Beside the chronostratigraphical interpretation of the succession, the composition and changes in ammonites faunas offer new data on their evolutionary development in relation to changing environment.\\u003c/p\\u003e\"},{\"header\":\"Description of the lithological succession\",\"content\":\"\\u003cp\\u003eFor the purpose of this study the whole succession of the Skork\\u0026oacute;w Lumachelle at Małogoszcz is subdivided into five units A-E (see Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig2\\\" class=\\\"InternalRef\\\"\\u003e2\\u003c/span\\u003e). The general faunal and lithological characters of the succession were given in several older studies (Kutek, \\u003cspan citationid=\\\"CR27\\\" class=\\\"CitationRef\\\"\\u003e1968\\u003c/span\\u003e; Kaźmierczak \\u0026amp; Pszcz\\u0026oacute;łkowski, \\u003cspan citationid=\\\"CR25\\\" class=\\\"CitationRef\\\"\\u003e1968\\u003c/span\\u003e; Seilacher et al., \\u003cspan citationid=\\\"CR45\\\" class=\\\"CitationRef\\\"\\u003e1985\\u003c/span\\u003e; Machalski, 1996; Matyja et al., \\u003cspan citationid=\\\"CR34\\\" class=\\\"CitationRef\\\"\\u003e2006\\u003c/span\\u003e; Matyja, \\u003cspan citationid=\\\"CR32\\\" class=\\\"CitationRef\\\"\\u003e2011\\u003c/span\\u003e), all of them have been taken into account along with some new observations when prepared the following description.\\u003c/p\\u003e \\u003cp\\u003eUnit A consists of thick-bedded, soft bioclastic limestones with numerous internal moulds of various infaunal bivalves, including those of \\u003cem\\u003ePholadomya\\u003c/em\\u003e, often preserved in life-position. There occur also commonly epifaunal bivalves like \\u003cem\\u003eActinostreon\\u003c/em\\u003e, \\u003cem\\u003eTrichites\\u003c/em\\u003e, \\u003cem\\u003eNanogyra\\u003c/em\\u003e and others, as well as various brachiopods and echinoids. The deposits attain 6.5 m in thickness. Their base is marked by the well-developed omission surface having character of hard-ground, and representing the successive stages of its development from soft- and firm-ground stages with numerous burrows (\\u003cem\\u003eThalassinoides\\u003c/em\\u003e and \\u003cem\\u003eRhizocorallium\\u003c/em\\u003e ) to bivalve and polychaete borings, and encrustation by serpulids of the hard-ground stage. This level marks the lower boundary of the Skork\\u0026oacute;w Lumachelle (or lumachelle/coquina formation) with the underlying \\u0026ldquo;sublithographic\\u0026rdquo; limestones of the Buczyna Limestone Mbr. of the Spinkowa G\\u0026oacute;ra Fm. (Wierzbowski, \\u003cspan citationid=\\\"CR49\\\" class=\\\"CitationRef\\\"\\u003e2020\\u003c/span\\u003e). Ammonite occur rather commonly, especially of the family Ataxioceratidae: \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e (\\u003cem\\u003eParataxioceras\\u003c/em\\u003e) to \\u0026ldquo;\\u003cem\\u003eOrthosphinctes\\u003c/em\\u003e(\\u003cem\\u003eArdescia\\u003c/em\\u003e)\\u0026rdquo;, \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eProgeronia\\u003c/em\\u003e, and of the family Aulacostephanidae: \\u003cem\\u003eEurasenia, Involuticeras, Prorasenia, Rasenia\\u003c/em\\u003e (\\u003cem\\u003ePachypictonia\\u003c/em\\u003e) (see Kutek, \\u003cspan citationid=\\\"CR27\\\" class=\\\"CitationRef\\\"\\u003e1968\\u003c/span\\u003e, \\u003cspan citationid=\\\"CR28\\\" class=\\\"CitationRef\\\"\\u003e1994\\u003c/span\\u003e; Matyja, Wierzbowski, \\u003cspan citationid=\\\"CR33\\\" class=\\\"CitationRef\\\"\\u003e2000\\u003c/span\\u003e; Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e; see also herein).\\u003c/p\\u003e \\u003cp\\u003eUnit B consists of oyster lumachelles about 2.5 m in thickness. The lumachelles are composed of densely packed shells of \\u003cem\\u003eActinostreon\\u003c/em\\u003e (\\u0026ldquo;\\u003cem\\u003eLopha\\u003c/em\\u003e\\u0026rdquo;, \\u0026ldquo;\\u003cem\\u003eAlectryonia\\u003c/em\\u003e\\u0026rdquo;) with marked admixture of other bivalve shells, and those of diverse other groups \\u0026ndash; brachiopods, gastropods, echinoids; additionally are found remains of starfish, crinoids, fish and others. The fossils are commonly overgrown by epizoans (sponges, serpulids, bryozoans) and bored by lithophags. The deposit reveals the features of non-deposition and winnowing of finer particles, as well as temporary reworking. The latter is shown e.g., by the occurrence of multiphase growth of oysters from the elongated forms attached to seminfaunal bivalve shells to the cup-shaped forms all of them preserved in deposit, but commonly not in life position; it is also the case of occurrence of disoriented internal moulds of deep burrowing bivalves, and clasts of coral colonies. All these features indicate the residual lag type character of the discussed deposit. The ammonites are fairly common \\u0026ndash; but usually fragmentarily preserved. These are especially represented by Ataxioceratidae: mostly \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e, less commonly \\u003cem\\u003eProgeronia\\u003c/em\\u003e, but to the virtual absence of \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e and \\u0026ldquo;\\u003cem\\u003eOrthosphinctes\\u003c/em\\u003e\\u0026rdquo;, and somewhat less abundantly by Aulacostephanidae: \\u003cem\\u003eEurasenia\\u003c/em\\u003e, \\u003cem\\u003eRasenia\\u003c/em\\u003e, \\u003cem\\u003eProrasenia\\u003c/em\\u003e (see Kutek, \\u003cspan citationid=\\\"CR27\\\" class=\\\"CitationRef\\\"\\u003e1968\\u003c/span\\u003e, \\u003cspan citationid=\\\"CR28\\\" class=\\\"CitationRef\\\"\\u003e1994\\u003c/span\\u003e; Matyja, Wierzbowski, \\u003cspan citationid=\\\"CR33\\\" class=\\\"CitationRef\\\"\\u003e2000\\u003c/span\\u003e; Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e, see also herein).\\u003c/p\\u003e \\u003cp\\u003eUnit C having only 1.75 m in thickness is developed as oncolitic limestone. Oncolites differ markedly in final size from less than millimeter to 3\\u0026ndash;4 cm, but the most commonly around 0.5-1 cm in diameter. The associated fauna is represented mostly by various bivalves, both infaunal to seminfaunal (often preserved in life position, such as \\u003cem\\u003ePleuromya\\u003c/em\\u003e) and epifaunal types (especially \\u003cem\\u003eNanogyra\\u003c/em\\u003e), associated with brachiopods, gastropods and echinoids. The ammonites occur fairly commonly. There is observed a marked domination of Ataxioceratidae: \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e, and \\u003cem\\u003eProgeronia\\u003c/em\\u003e, and less common occurrence of Aulacostephanidae: mostly \\u003cem\\u003eProrasenia\\u003c/em\\u003e, subordinately \\u003cem\\u003eInvoluticeras\\u003c/em\\u003e and \\u003cem\\u003eEurasenia\\u003c/em\\u003e, but also of Aspidoceratidae: \\u003cem\\u003ePseudhimalayites\\u003c/em\\u003e and \\u003cem\\u003ePsedowaagenia\\u003c/em\\u003e (see detailed comments below).\\u003c/p\\u003e \\u003cp\\u003eUnit D, attaining 8.25 m in thickness, consists of lumachelles with \\u003cem\\u003eNanogyra\\u003c/em\\u003e: these are composed of \\u003cem\\u003eNanogyra\\u003c/em\\u003e shells and their hash occurring in micritic limestone or marly matrix; the deposits are well-bedded with intervening beds of micritic limestones and marls, especially common in the middle part of the unit. The faunal assemblage is rather monotonous, dominated by epifaunal oysters \\u003cem\\u003eNanogyra\\u003c/em\\u003e, less commonly serpulids, crinoids, echinoids, starfish. The overlying deposits of unit E, 5.50 m in thickness, are thick-bedded bioclastic limestones with numerous internal moulds of various infaunal bivalves, including those of \\u003cem\\u003ePholadomya\\u003c/em\\u003e, intervening in the middle by a prominent marly bed without macrofana. A highest bed of limestones of unit E yielded numerous specimens of aspidoceratid ammonite \\u003cem\\u003ePseudhimalayites.\\u003c/em\\u003e The collection of ammonites coming from units D and E is, however, treated jointly, because of difficulties in proper location of some collected ammonites. It is composed of occurring mostly in nearly equal proportions Ataxioceratidae (\\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e, \\u003cem\\u003eTolvericeras\\u003c/em\\u003e, \\u003cem\\u003eProgeronia\\u003c/em\\u003e) and Aspidoceras (\\u003cem\\u003ePseudhimalayites\\u003c/em\\u003e, very commonly). Some specimens of Aulacostephanidae represent a very diversified assemblage ( \\u003cem\\u003eProrasenia\\u003c/em\\u003e, \\u003cem\\u003eRasenia\\u003c/em\\u003e, \\u003cem\\u003eRasenioides\\u003c/em\\u003e, and possibly \\u003cem\\u003ePararasenia\\u003c/em\\u003e) (Kutek, \\u003cspan citationid=\\\"CR27\\\" class=\\\"CitationRef\\\"\\u003e1968\\u003c/span\\u003e; Matyja, Wierzbowski, \\u003cspan citationid=\\\"CR33\\\" class=\\\"CitationRef\\\"\\u003e2000\\u003c/span\\u003e; Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e; see also comments below). A few large specimens of phylloceratids attaining about 0.5 m in diameter discovered in an upper part of unit E represent possibly allochtonous post-mortem drifted shells.\\u003c/p\\u003e \\u003cdiv id=\\\"Sec3\\\" class=\\\"Section2\\\"\\u003e \\u003ch2\\u003eStratigraphical and palaeobiogeographical interpretation of the ammonite faunas\\u003c/h2\\u003e \\u003cp\\u003eThe studied ammonite faunas contain besides the dominating Submediterranean-Mediterranean forms, also fairly commonly the Subboreal ones, as well as some of the strictly Mediterranean origin. Such a spectrum of ammonites enables not only the recognition of the various biostratigraphical zonations, but also makes possible correlation between the particular zonal schemes of different bioprovinces.\\u003c/p\\u003e \\u003cp\\u003eThe ammonites of the family Ataxioceratidae are the typical Submediterranean (partly also Mediterranean) forms. Although \\u0026ldquo;the family is still one of the most difficult to classify\\u0026rdquo; ( Enay \\u0026amp; Howarth, \\u003cspan citationid=\\\"CR13\\\" class=\\\"CitationRef\\\"\\u003e2019\\u003c/span\\u003e, p. 112; see also discussion in chapter on evolution), its differentiation has became the basis for foundation of the Submediterranean zonations of the Lower Kimmeridgian, especially that established in south-eastern France, in the Jura Mts. in Switzerland, and in Swabian Alb and Franconian Alb in southern Germany (see e.g., Geyer, \\u003cspan citationid=\\\"CR18\\\" class=\\\"CitationRef\\\"\\u003e1961\\u003c/span\\u003e; Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e; Gygi, \\u003cspan citationid=\\\"CR19\\\" class=\\\"CitationRef\\\"\\u003e2003\\u003c/span\\u003e; Enay et al., \\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e), which is evidently recognizable in the area of central Poland (e.g., Kutek, \\u003cspan citationid=\\\"CR27\\\" class=\\\"CitationRef\\\"\\u003e1968\\u003c/span\\u003e), including the section studied. The ammonites studied herein can be attributed to three different groups. The first of them recognized only in unit A in the Małogoszcz section is closely related to the genus \\u003cem\\u003eAtaxioceras.\\u003c/em\\u003e It is represented by \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e (\\u003cem\\u003eParataxioceras\\u003c/em\\u003e) cf. \\u003cem\\u003eplanulatum\\u003c/em\\u003e (Quenstedt) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig3\\\" class=\\\"InternalRef\\\"\\u003e3\\u003c/span\\u003ea), \\u003cem\\u003eA.\\u003c/em\\u003e (\\u003cem\\u003eP.\\u003c/em\\u003e) \\u003cem\\u003eoppeli parvum\\u003c/em\\u003e Atrops (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig3\\\" class=\\\"InternalRef\\\"\\u003e3\\u003c/span\\u003eb), and \\u0026ldquo;\\u003cem\\u003eOrthosphinctes\\u003c/em\\u003e (\\u003cem\\u003eArdescia\\u003c/em\\u003e)\\u0026rdquo; \\u003cem\\u003eperayensis\\u003c/em\\u003e Atrops (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig3\\\" class=\\\"InternalRef\\\"\\u003e3\\u003c/span\\u003ec). The representatives of \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e are indicative of the \\u003cem\\u003esemistriatum\\u003c/em\\u003e horizon, possibly beginning from its base as suggests occurrence of a form similar to \\u003cem\\u003eA. planulatum\\u003c/em\\u003e characteristic of still older \\u003cem\\u003ehypselocyclum\\u003c/em\\u003e horizon, of the upper part of the Lothari Subzone of the Hypselocyclum Zone in the accepted herein subdivision of Atrops (\\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e). The occurrence of \\u0026ldquo;\\u003cem\\u003eO\\u003c/em\\u003e\\u0026rdquo;. \\u003cem\\u003eperayensis\\u003c/em\\u003e, being a form of the \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e (\\u003cem\\u003eParataxioceras\\u003c/em\\u003e) \\u003cem\\u003eoppeli\\u003c/em\\u003e group, possibly reduced in ontogenetic development due to the heterochrony, is indicative moreover of the topmost part of the Hypselocyclum Zone (Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e; see also comments on evolution below). The stratigraphical interpretation of all these ammonites is consistent with the occurrence of \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e and \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e of the second group of Ataxioceratidae in the discussed ammonite fauna of unit A. Both these genera appear for the first time in the Submediterranean succession in the \\u003cem\\u003esemistriatum\\u003c/em\\u003e horizon of the Hypselocyclum Zone (Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e). Of the recognized here three species of that group \\u0026ndash; \\u003cem\\u003eG. melliconense\\u003c/em\\u003e (Geyer) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig3\\\" class=\\\"InternalRef\\\"\\u003e3\\u003c/span\\u003ed), \\u003cem\\u003eCrussoliceras sayni\\u003c/em\\u003e (Camus et Thieuloy) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig4\\\" class=\\\"InternalRef\\\"\\u003e4\\u003c/span\\u003ea), and \\u003cem\\u003eGarnierisphinctes garnieri\\u003c/em\\u003e (Fontannes) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig4\\\" class=\\\"InternalRef\\\"\\u003e4\\u003c/span\\u003eb)\\u0026ndash; the middle has been reported from the upper part of the Lothari Subzone (Gygi, \\u003cspan citationid=\\\"CR19\\\" class=\\\"CitationRef\\\"\\u003e2003\\u003c/span\\u003e), whereas the level of appearance of the latter two has not been so far precisely recognized. The genus \\u003cem\\u003eProgeronia\\u003c/em\\u003e of the third group of Ataxioceratidae is represented in unit A both by macroconchs: \\u003cem\\u003eProgeronia\\u003c/em\\u003e (\\u003cem\\u003eProgeronia\\u003c/em\\u003e) \\u003cem\\u003eprogeron\\u003c/em\\u003e (von Ammon) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig5\\\" class=\\\"InternalRef\\\"\\u003e5\\u003c/span\\u003ea) and \\u003cem\\u003eP.\\u003c/em\\u003e (\\u003cem\\u003eP.\\u003c/em\\u003e) cf. \\u003cem\\u003eeggeri\\u003c/em\\u003e (von Ammon), and microconch \\u003cem\\u003eProgeronia\\u003c/em\\u003e (\\u003cem\\u003eHugueninsphinctes\\u003c/em\\u003e) \\u003cem\\u003ebreviceps\\u003c/em\\u003e (Quenstedt) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig5\\\" class=\\\"InternalRef\\\"\\u003e5\\u003c/span\\u003eb). Although the appearance of \\u003cem\\u003eProgeronia\\u003c/em\\u003e in the upper part of the Hypselocyclum Zone has been commonly recognized (e.g., Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e), the reported new findings for the first time firmly prove the occurrence of the discussed species at that stratigraphical level.\\u003c/p\\u003e\\u003cp\\u003eThe ammonites coming from unit B do not reveal the representatives of the first group related to the genus \\u003cem\\u003eAtaxioceras.\\u003c/em\\u003e Instead there are commonly represented forms of two other groups of Ataxioceratidae: \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e and \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e ones, as well as that of the genus \\u003cem\\u003eProgeronia.\\u003c/em\\u003e Unfortunately because of the taphonomic reasons (see above) the specimens are mostly incomplete and difficult for closer determination. The only recognized specifically forms are: \\u003cem\\u003eGarnieriphinctes\\u003c/em\\u003e cf. \\u003cem\\u003egarnieri\\u003c/em\\u003e (Fontannes) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig3\\\" class=\\\"InternalRef\\\"\\u003e3\\u003c/span\\u003ee) and \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e cf. \\u003cem\\u003eaceroides\\u003c/em\\u003e Geyer (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig4\\\" class=\\\"InternalRef\\\"\\u003e4\\u003c/span\\u003ec-d). Nevertheless, the assemblage is diagnostic of the lower part of the Divisum Zone \\u0026ndash; and may be treated as corresponding to the Crusoliensis or Tenuicostatum Subzone according to stratigraphical interpretation accepted herein (see e.g., Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e; Enay et al., \\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eIt should be remembered, however, that in stratigraphical scheme of similar Submediterranean succession of southern Germany, the lower boundary of the Divisum Zone has been originally correlated with the level of the first occurrence of \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e and \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e (e.g., Geyer, \\u003cspan citationid=\\\"CR18\\\" class=\\\"CitationRef\\\"\\u003e1961\\u003c/span\\u003e). According to that stratigrapical subdivision, the whole interval corresponding to unit A in the Małogoszcz section (compared with the upper part of the Lothari Subzone herein) would be correlated already with the lowest part of the Divisum Zone.\\u003c/p\\u003e \\u003cp\\u003eOn the other hand, a markedly different ammonite succession is recognized in the coeval deposits of the Spanish sections of the Iberian Range, which can treated as representative of the western part of Submediterranean Province. It includes the occurrence there of a special ataxiocertid group distinguished as corresponding to the new genus \\u003cem\\u003eGeyericeras\\u003c/em\\u003e, not known in other European areas. These ammonites define the \\u003cem\\u003earagoniense\\u003c/em\\u003e stratigraphical horizon occurring directly below the appearance of \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e indicating already the base of the Divisum Zone. The relevant correlation with SE France and eastern parts of the Submediterranean Province, including central Poland, strongly suggests the position of the \\u003cem\\u003earagoniense\\u003c/em\\u003e horizon directly below the upper part of the \\u003cem\\u003esemistriatum\\u003c/em\\u003e horizon and the \\u003cem\\u003eperayensis\\u003c/em\\u003e horizon (see Moliner \\u0026amp; Ol\\u0026oacute;riz, \\u003cspan citationid=\\\"CR36\\\" class=\\\"CitationRef\\\"\\u003e2009\\u003c/span\\u003e, \\u003cspan citationid=\\\"CR37\\\" class=\\\"CitationRef\\\"\\u003e2010\\u003c/span\\u003e; see also Moliner, \\u003cspan citationid=\\\"CR36\\\" class=\\\"CitationRef\\\"\\u003e2009\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eThe ataxioceratid ammonites from unit C of the Małogoszcz section are still markedly dominated by \\u003cem\\u003eGarnierishinctes\\u003c/em\\u003e and \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, although the species are mostly different when compared with older units: \\u003cem\\u003eGarnierisphinctes semigarnieri\\u003c/em\\u003e (Geyer) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig6\\\" class=\\\"InternalRef\\\"\\u003e6\\u003c/span\\u003ea), \\u003cem\\u003eG. championneti\\u003c/em\\u003e (Fontannes) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig6\\\" class=\\\"InternalRef\\\"\\u003e6\\u003c/span\\u003eb), \\u003cem\\u003eG. plebejus\\u003c/em\\u003e (Neumayr) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig6\\\" class=\\\"InternalRef\\\"\\u003e6\\u003c/span\\u003ec), as well as \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e cf. \\u003cem\\u003elacertosum\\u003c/em\\u003e (Fontannes), \\u003cem\\u003eC.\\u003c/em\\u003e cf. \\u003cem\\u003eatavum\\u003c/em\\u003e (Schneid) \\u0026ndash; \\u003cem\\u003eaceroides\\u003c/em\\u003e (Geyer). It is worth noting also the first occurrence of a form which possibly can be referred to the genus \\u003cem\\u003eTolvericeras\\u003c/em\\u003e; the corresponding specimens (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig6\\\" class=\\\"InternalRef\\\"\\u003e6\\u003c/span\\u003ed) are very similar to that described as \\u0026ldquo;\\u003cem\\u003eTolvericeras\\u003c/em\\u003e (\\u003cem\\u003eTolvericeras\\u003c/em\\u003e) n. sp.\\u0026rdquo; by Gygi (\\u003cspan citationid=\\\"CR19\\\" class=\\\"CitationRef\\\"\\u003e2003\\u003c/span\\u003e, Figs.\\u0026nbsp;165\\u0026ndash;166) showing the polygyrate subdivision of ribs placed low in the whorl-side; this form was treated subsequently as taking the intermediate position between \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eTolvericeras\\u003c/em\\u003e (Enay et al., \\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e, p. 327). Some representatives of \\u003cem\\u003eProgeronia\\u003c/em\\u003e with well preserved specimen of \\u003cem\\u003eProgeronia\\u003c/em\\u003e (\\u003cem\\u003eHugueninsphinctes\\u003c/em\\u003e) \\u003cem\\u003ebreviceps\\u003c/em\\u003e (Quenstedt) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig5\\\" class=\\\"InternalRef\\\"\\u003e5\\u003c/span\\u003ec) are also recognized. The occurrence of several specimens of Aspidoceratidae represented mostly by \\u003cem\\u003ePseudohimalayites uhlandi\\u003c/em\\u003e (Oppel) unequivocally indicates that the whole ammonite assemblage from unit C corresponds already to the Uhlandi Subzone of the upper part of the Divisum Zone (see e.g., Geyer, \\u003cspan citationid=\\\"CR18\\\" class=\\\"CitationRef\\\"\\u003e1961\\u003c/span\\u003e).\\u003c/p\\u003e\\u003cp\\u003eThe last ataxioceratid ammonites coming from units D and E are dominated by representatives of \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e: \\u003cem\\u003eC.\\u003c/em\\u003e cf. \\u003cem\\u003ecrusoliense\\u003c/em\\u003e (Fontannes); \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e: \\u003cem\\u003eG. championneti\\u003c/em\\u003e (Fontannes); and \\u003cem\\u003eTolvericeras\\u003c/em\\u003e group; the representatives of the \\u003cem\\u003eProgeronia\\u003c/em\\u003e group: \\u003cem\\u003eProgeronia\\u003c/em\\u003e (\\u003cem\\u003eProgeronia\\u003c/em\\u003e) cf. \\u003cem\\u003eeggeri\\u003c/em\\u003e (von Ammon) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig5\\\" class=\\\"InternalRef\\\"\\u003e5\\u003c/span\\u003ed) are less common. On the other hand, very numerously occur Aspidoceratidae represented almost exclusively by \\u003cem\\u003ePsudhimalayites uhlandi\\u003c/em\\u003e (Oppel). These ammonites represent the upper parts of the Uhlandi Subzone of the Divisum Zone.\\u003c/p\\u003e \\u003cp\\u003eSeveral ammonites of the families Ataxioceratidae (such as \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eProgeronia\\u003c/em\\u003e), as well as of Aspidoceratidae (mostly \\u003cem\\u003ePseudhimalayites\\u003c/em\\u003e) occurring in the studied succession of the Holy Cross Mts., central Poland, are in common with areas of the Mediterranean Province such as the Venetian Alps (see e.g., Pavia et al., \\u003cspan citationid=\\\"CR39\\\" class=\\\"CitationRef\\\"\\u003e1987\\u003c/span\\u003e; Sarti, \\u003cspan citationid=\\\"CR41\\\" class=\\\"CitationRef\\\"\\u003e1993\\u003c/span\\u003e; Caracuel et al., \\u003cspan citationid=\\\"CR9\\\" class=\\\"CitationRef\\\"\\u003e1998\\u003c/span\\u003e), and the Central Appenines (Cecca et al., \\u003cspan citationid=\\\"CR11\\\" class=\\\"CitationRef\\\"\\u003e1985\\u003c/span\\u003e; Cecca \\u0026amp; Santantonio, \\u003cspan citationid=\\\"CR10\\\" class=\\\"CitationRef\\\"\\u003e1986\\u003c/span\\u003e) in Italy, the Betic Cordillera in southern Spain (Ol\\u0026oacute;riz, \\u003cspan citationid=\\\"CR38\\\" class=\\\"CitationRef\\\"\\u003e1978\\u003c/span\\u003e), the Gerecse-Pils Moutains and the Bakony Mountains in Hungary (Főzy \\u0026amp; Scherzinger, \\u003cspan citationid=\\\"CR15\\\" class=\\\"CitationRef\\\"\\u003e2013\\u003c/span\\u003e; Főzy et al., \\u003cspan citationid=\\\"CR16\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e), the Romanian Carpathians (e.g., Grigore, \\u003cspan citationid=\\\"CR17\\\" class=\\\"CitationRef\\\"\\u003e2000\\u003c/span\\u003e), and the Balkan Mts. in Bulgaria (Sapunov, \\u003cspan citationid=\\\"CR42\\\" class=\\\"CitationRef\\\"\\u003e1979\\u003c/span\\u003e). This along with occurrence in the succession studied of some strictly Tethyan ammonites, such as \\u003cem\\u003ePresimoceras\\u003c/em\\u003e, \\u003cem\\u003eIdoceras\\u003c/em\\u003e and \\u003cem\\u003eNebrodites\\u003c/em\\u003e allows for recognition of the Mediterranean zonation (see Sarti, \\u003cspan citationid=\\\"CR41\\\" class=\\\"CitationRef\\\"\\u003e1993\\u003c/span\\u003e; Caracuel et al., \\u003cspan citationid=\\\"CR9\\\" class=\\\"CitationRef\\\"\\u003e1998\\u003c/span\\u003e, and correlations with older subdivisions).\\u003c/p\\u003e \\u003cp\\u003eThe ammonites of the genus \\u003cem\\u003ePresimoceras\\u003c/em\\u003e occur rarely in unit B of the Małogoszcz section. They are fragmentarily preserved, nevertheless they can be attributed to the \\u003cem\\u003eP. herbichi\\u003c/em\\u003e group (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003eg-h-i), being possibly close to \\u003cem\\u003eP. nodulatum\\u003c/em\\u003e (Quenstedt). Such taxonomical interpretation indicates the correlation with the Mediterranean Herbichi Zone, additionally because of common occurrence of \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e - with its middle part \\u0026ndash; the Divisum Subzone (see Sarti, \\u003cspan citationid=\\\"CR41\\\" class=\\\"CitationRef\\\"\\u003e1993\\u003c/span\\u003e). The occurrence of a single specimen of \\u003cem\\u003eIdoceras balderum\\u003c/em\\u003e (Oppel) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003ek) in the discussed unit B suggests also similar correlation. Although the typical forms of \\u003cem\\u003eI. balderum\\u003c/em\\u003e are commonly referred to the upper part of the Divisum Zone in Submediterranean Province (SE France, southern Germany, see e.g., Geyer, \\u003cspan citationid=\\\"CR18\\\" class=\\\"CitationRef\\\"\\u003e1961\\u003c/span\\u003e; Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e; see also Schweigert \\u0026amp; Kuschel, \\u003cspan citationid=\\\"CR44\\\" class=\\\"CitationRef\\\"\\u003e2017\\u003c/span\\u003e), some specimens coming from a lower part of the Divisum Zone in other areas (Swiss Jura Mts., Venetian Alps, Italy) are compared with that species as well (see e.g., Gygi \\u0026amp; Persoz, \\u003cspan citationid=\\\"CR20\\\" class=\\\"CitationRef\\\"\\u003e1986\\u003c/span\\u003e; Pavia et al., \\u003cspan citationid=\\\"CR39\\\" class=\\\"CitationRef\\\"\\u003e1987\\u003c/span\\u003e; Sarti, \\u003cspan citationid=\\\"CR41\\\" class=\\\"CitationRef\\\"\\u003e1993\\u003c/span\\u003e). The overlying deposits of unit C yielded a few specimens of \\u003cem\\u003eNebrodites\\u003c/em\\u003e including \\u003cem\\u003eN. favaraenenis\\u003c/em\\u003e (Gemmellaro) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003ef) and \\u003cem\\u003eN.\\u003c/em\\u003e cf. \\u003cem\\u003eagrigentinus\\u003c/em\\u003e (Gemmellaro) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003ej), which together with appearance of \\u003cem\\u003ePseudhimalayites uhlandi\\u003c/em\\u003e (Oppel) indicate the upper part of the Herbichi Zone \\u0026ndash; the Uhlandi Subzone (see Sarti, \\u003cspan citationid=\\\"CR41\\\" class=\\\"CitationRef\\\"\\u003e1993\\u003c/span\\u003e). Similarly, the co-occurrence of \\u003cem\\u003eP. uhlandi\\u003c/em\\u003e with \\u003cem\\u003eNebrodites\\u003c/em\\u003e sp. and \\u003cem\\u003eTaramelliceras\\u003c/em\\u003e (\\u003cem\\u003eTaramelliceras\\u003c/em\\u003e) \\u003cem\\u003ecompsum\\u003c/em\\u003e (Oppel) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003el) as recognized in still higher units units D and E indicates the presence of some upper parts of the Uhlandi Subzone (see Caracuel et al., \\u003cspan citationid=\\\"CR9\\\" class=\\\"CitationRef\\\"\\u003e1998\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eSome problem arises with interpretation in term of the Mediterranean zonation of the lowest part of the studied succession \\u0026ndash; unit A of the Małogoszcz section, corresponding in the Submediterranean subdivision to the uppermost part of the Hypselocyclum Zone and the upper part of the Lothari Subzone. The only ammonite of a strictly Mediterranean character coming from that stratigraphical interval is \\u003cem\\u003eNebrodites maccerimus\\u003c/em\\u003e (Quenstedt) (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003ee), according to interpretation of the species by Ziegler (1959). Just that species was reported, however, from the boundary beds of the two Mediterranean zones \\u0026ndash; the Strombecki Zone and the Herbichi Zone or corresponding beds of the Divisum Zone (Caracuel et al., \\u003cspan citationid=\\\"CR9\\\" class=\\\"CitationRef\\\"\\u003e1998\\u003c/span\\u003e; see also Ol\\u0026oacute;riz, \\u003cspan citationid=\\\"CR38\\\" class=\\\"CitationRef\\\"\\u003e1978\\u003c/span\\u003e; Sapunov, \\u003cspan citationid=\\\"CR42\\\" class=\\\"CitationRef\\\"\\u003e1979\\u003c/span\\u003e). This, together with observations given above, suggests the discussed unit A corresponds most probably to the lowermost part of the Herbichi Zone.\\u003c/p\\u003e \\u003cp\\u003eThe ammonite faunas of the family Aulacostephanidae commonly represented in the succession studied are indicative of the Subboreal Province. These ammonites numerously occurring in units A to B, less commonly in unit C, are mostly belonging to the genera \\u003cem\\u003eEurasenia\\u003c/em\\u003e and \\u003cem\\u003eInvoluticeras\\u003c/em\\u003e of the north-eastern European branch of the family, and rarely to the genus \\u003cem\\u003eRasenia\\u003c/em\\u003e (and its local ally \\u003cem\\u003ePachypictonia\\u003c/em\\u003e) related to its north-western European branch (Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e); both these groups of macroconchs occur together with their microconch counterparts of the genus \\u003cem\\u003eProrasenia\\u003c/em\\u003e. Some of these ammonites were presented and discussed previously: \\u003cem\\u003eRasenia\\u003c/em\\u003e (\\u003cem\\u003ePachypictonia\\u003c/em\\u003e) aff. \\u003cem\\u003eindicatoria\\u003c/em\\u003e (Schneid), which seems to be related to \\u003cem\\u003eRasenia evoluta\\u003c/em\\u003e Spath (Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e, pl. 7), \\u003cem\\u003eEurasenia rolandi\\u003c/em\\u003e (Oppel) (Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e, pl. 10:4), and \\u003cem\\u003eE. trimera\\u003c/em\\u003e (Oppel) (Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e, pl. 11: 4) as well as \\u003cem\\u003eInvoluticeras involutum\\u003c/em\\u003e (Quenstedt) (Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e, pl. 14: 2) \\u0026ndash; all of them from unit A; \\u003cem\\u003eEurasenia pendula\\u003c/em\\u003e (Schneid) (Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e, pl. 11: 2\\u0026ndash;3) \\u0026ndash; from unit B; and \\u003cem\\u003eEurasenia trimera\\u003c/em\\u003e (Oppel) (Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e, pl. 11: 5), possibly from unit C. In addition, several specimens of \\u003cem\\u003eE. trimera\\u003c/em\\u003e (Oppel), \\u003cem\\u003eE. trifurcata\\u003c/em\\u003e (Reinecke), \\u003cem\\u003eE. pendula\\u003c/em\\u003e (Schneid), associated with \\u003cem\\u003eInvoluticeras\\u003c/em\\u003e, including \\u003cem\\u003eI. crassicostatum\\u003c/em\\u003e (Geyer), along with common \\u003cem\\u003eProrasenia\\u003c/em\\u003e \\u0026ndash; especially \\u003cem\\u003eP. quenstedti\\u003c/em\\u003e Schindewolf and \\u003cem\\u003eP. witteana\\u003c/em\\u003e (Oppel), are reported from units A to C. On the other hand, some specimens of the genus \\u003cem\\u003eRasenia\\u003c/em\\u003e, including form similar to \\u003cem\\u003eR. involuta\\u003c/em\\u003e Spath (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003ea-b), have been recognized in units B and D-E (near the top of the section).\\u003c/p\\u003e \\u003cp\\u003eSummarizing, the ammonites of the genera \\u003cem\\u003eEurasenia\\u003c/em\\u003e and \\u003cem\\u003eInvoluticeras\\u003c/em\\u003e (associated with \\u003cem\\u003eProrasenia\\u003c/em\\u003e microconchs) occur in units A-C in the Małogoszcz section, indicating a stronger NE Subboreal influences, whereas NW Subboreal \\u003cem\\u003eRasenia\\u003c/em\\u003e are sporadically encountered nearly throughout the whole succession up to its top. Additionally, a few fragmentarily preserved specimens from unit E (and possibly its upper part), showing the ribbing similar to that of \\u003cem\\u003eEurasenia\\u003c/em\\u003e, reveal some weakening of ornamentation on the ventral side of whorls resembling thus younger genus \\u003cem\\u003ePararasenia\\u003c/em\\u003e (see Ziegler, \\u003cspan citationid=\\\"CR53\\\" class=\\\"CitationRef\\\"\\u003e1962\\u003c/span\\u003e). They are especially similar to \\u003cem\\u003eP. quenstedti\\u003c/em\\u003e Durand, differing in more elongated primary ribs, and in a weaker development of the ventral smooth band: thus, they are referred herein to as ? \\u003cem\\u003ePararasenia\\u003c/em\\u003e aff. \\u003cem\\u003equenstedti\\u003c/em\\u003e Durand (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003ec-d). Moreover, in the upper part of the succession there appear rarely ammonites of the genus \\u003cem\\u003eRasenioides\\u003c/em\\u003e, representing a different branch of Aulacostephanidae, such as \\u003cem\\u003eR. moeschi\\u003c/em\\u003e (Oppel), coming from the lowermost part of unit D, and illustrated by Matyja \\u0026amp; Wierzbowski (\\u003cspan citationid=\\\"CR33\\\" class=\\\"CitationRef\\\"\\u003e2000\\u003c/span\\u003e, Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig4\\\" class=\\\"InternalRef\\\"\\u003e4\\u003c/span\\u003ec) and Wierzbowski (\\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e, pl. 15:2A-B), and some other poorly preserved and difficult for closer determination specimens of that genus currently recognized in units D-E.\\u003c/p\\u003e \\u003cp\\u003eThe stratigraphical interpretation of the discussed Subboreal ammonites in term of the Subboreal zonation indicates the correlation of the whole discussed succession with the NW European Cymodoce Zone. The occurrence of ammonites similar to \\u003cem\\u003eRasenia evoluta\\u003c/em\\u003e and \\u003cem\\u003eR. involuta\\u003c/em\\u003e, strongly suggests the presence of the higher levels of that zone (see Birkelund et al., \\u003cspan citationid=\\\"CR4\\\" class=\\\"CitationRef\\\"\\u003e1978\\u003c/span\\u003e, \\u003cspan citationid=\\\"CR5\\\" class=\\\"CitationRef\\\"\\u003e1983\\u003c/span\\u003e). It should be remembered, however, that the highest part of the Cymodoce Zone was often treated in the past as an interval characterized by common occurrence of the fine-ribbed \\u003cem\\u003eRasenioides.\\u003c/em\\u003e In the studied succession at Małogoszcz, dominated by Submediterranean ammonites, the Subboreal \\u003cem\\u003eRasenioides\\u003c/em\\u003e ammonites are very rare, which precludes the precise differentiation of stratigraphical intervals corresponding to the Askepta Subzone, and/or Chatelaillonensis Subzone \\u0026ndash; both defined by occurrence of the \\u003cem\\u003eRasenioides\\u003c/em\\u003e faunas in northern European areas (see Birkelund et al., \\u003cspan citationid=\\\"CR5\\\" class=\\\"CitationRef\\\"\\u003e1983\\u003c/span\\u003e; Hantzpergue, \\u003cspan citationid=\\\"CR21\\\" class=\\\"CitationRef\\\"\\u003e1989\\u003c/span\\u003e, \\u003cspan citationid=\\\"CR22\\\" class=\\\"CitationRef\\\"\\u003e1995\\u003c/span\\u003e). The former can be possibly correlated with the bulk of the succession studied from the Submediterranean horizon \\u003cem\\u003eperayensis\\u003c/em\\u003e at its base, whereas the base of the latter subzone runs possibly somewhat lower, near the base of the \\u003cem\\u003esemistriatum\\u003c/em\\u003e horizon, as resulted from wider biostratigraphical correlations of the Subboreal and Submediterranean sections (see Matyja, Wierzbowski, \\u003cspan citationid=\\\"CR33\\\" class=\\\"CitationRef\\\"\\u003e2000\\u003c/span\\u003e; Comment et al., \\u003cspan citationid=\\\"CR12\\\" class=\\\"CitationRef\\\"\\u003e2015\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003e \\u003cb\\u003eChanges in environment\\u003c/b\\u003e \\u003cb\\u003eversus\\u003c/b\\u003e \\u003cb\\u003eevolutionary development of ammonites\\u003c/b\\u003e\\u003c/p\\u003e \\u003cp\\u003eThe stratigraphical interval corresponding to the upper part of the Hypselocyclum Zone and to the Divisum Zone (or in a broader sense to the whole Divisum Zone) of the uppermost Lower Kimmeridgian represents one of the most prominent faunal turnover in the whole Upper Jurassic. It is markedly correlated with changes in the depositional environment as based on sedimentological data. The main reasons of changes were of climatic and tectonic nature resulting from sea-level oscillations, and/or opening of new sea-routs. It should be remembered that the deepest faunal changes generally occurred during the transgressions, whereas endemism was rather related to dominance of the shallow-water environments (Atrops \\u0026amp; Ferry, \\u003cspan citationid=\\\"CR2\\\" class=\\\"CitationRef\\\"\\u003e1989\\u003c/span\\u003e; Hanzpergue, 1995; Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eThe stratigraphical interval discussed herein corresponded in the Submediterranean Province to decline of the shallow-water carbonate platforms due to progress of a large transgression. This resulted from the tectonic subsidence of the wide shallow-water carbonate areas including that of the Holy Cross Mountains in central Poland: at the boundary between the COK and the LUK tectono-stratigraphic sequences (Kutek, \\u003cspan citationid=\\\"CR28\\\" class=\\\"CitationRef\\\"\\u003e1994\\u003c/span\\u003e) which corresponds to the boundary between the Buczyna Mbr. of the Spinkowa G\\u0026oacute;ra Fm., and the Skork\\u0026oacute;w Lumachelle of the Coquina Fm. in the Małogoszcz section (Wierzbowski, \\u003cspan citationid=\\\"CR49\\\" class=\\\"CitationRef\\\"\\u003e2020\\u003c/span\\u003e). The progress of the transgression is well shown in the section studied by several sedimentological observation summarized by Matyja et al. (\\u003cspan citationid=\\\"CR34\\\" class=\\\"CitationRef\\\"\\u003e2006\\u003c/span\\u003e), and by analysis of the geochemical data, mostly oxygen and carbon composition of shells of various oysters by Wierzbowski (\\u003cspan citationid=\\\"CR51\\\" class=\\\"CitationRef\\\"\\u003e2019\\u003c/span\\u003e). A similar tectonic phenomenon is observed in the development of the Bann\\u0026eacute; Member of the Lower Reuchenette Fm. in the Jura Mountains of northern Switzerland which marks the change from an older flat carbonate platform topography into that of a \\u0026ldquo;prominent basin and swell morphology\\u0026rdquo; (Jank et al., \\u003cspan citationid=\\\"CR24\\\" class=\\\"CitationRef\\\"\\u003e2006\\u003c/span\\u003e). In addition, the climatic oscillations had also a marked influence on sea-level changes, especially those of longer duration related to 100-kyr and 405-kyr eccentricity cycles. Such a study to attempt to recognize the climatic cycles was presented on the basis of detailed geochemical analysis of the Early Kimmeridgian pelagic deposits of the south-eastern France having a good ammonite stratigraphy (Boulila et al., \\u003cspan citationid=\\\"CR6\\\" class=\\\"CitationRef\\\"\\u003e2008\\u003c/span\\u003e; see also Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e). It resulted in recognition of three main eccentricity cycles within deposits strictly coeval to those studied herein and showing similar assemblage of ammonites: beginning with the important transgressive level corresponding to minimum of 405-kyr MS cycle developed at the base of the whole succession (Min. 4 in Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig2\\\" class=\\\"InternalRef\\\"\\u003e2\\u003c/span\\u003e of Boulila et al., \\u003cspan citationid=\\\"CR6\\\" class=\\\"CitationRef\\\"\\u003e2008\\u003c/span\\u003e), and the following two minima of 100-kyr cycles. The duration of the whole stratigraphical interval corresponding to the broadly treated Divisum Zone can be estimated as 260 to 300 kyr (Boulila et al., \\u003cspan citationid=\\\"CR6\\\" class=\\\"CitationRef\\\"\\u003e2008\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eThe overall transgression at the decline of the Early Kimmeridgian attained its very high level in central Poland (and south-eastern France) at the end of the Hypselocyclum Chron \\u0026ndash; during the \\u003cem\\u003esemistriatum\\u003c/em\\u003e and \\u003cem\\u003eperayenis\\u003c/em\\u003e horizons, when the transgressive deposits of a basal part of the Skork\\u0026oacute;w Lumachelle (denoted herein as unit A, see Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig2\\\" class=\\\"InternalRef\\\"\\u003e2\\u003c/span\\u003e) completely covered the earlier shallow-water carbonate platform deposits. This level additionally corresponds to the minimum (Min. 4 after Boulila et al., \\u003cspan citationid=\\\"CR6\\\" class=\\\"CitationRef\\\"\\u003e2008\\u003c/span\\u003e) of the 405-kyr eccentricity cycle: it marks the minimum of the magnetic susceptibility (MS), and corresponds to enhanced carbonate production, showing the maximum insolation, which appears to have induced a very high sea-level according to the model proposed by Boulila et al. (\\u003cspan citationid=\\\"CR6\\\" class=\\\"CitationRef\\\"\\u003e2008\\u003c/span\\u003e, \\u003cspan citationid=\\\"CR7\\\" class=\\\"CitationRef\\\"\\u003e2010\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eThe transgression in the Submediterranean Province controlled both by climatic and synsedimentary tectonics resulted in a marked exchange of the ammonite faunas (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig8\\\" class=\\\"InternalRef\\\"\\u003e8\\u003c/span\\u003e). The extinction of the older lineage of typical Submediterranean ammonites Ataxioceratinae, corresponding to decline of the genus \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e, was associated with the appearance of new members of the family Ataxioceratidae, such as genera \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e and \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e, beginning a new evolutionary stage of their development (see Atrops \\u0026amp; Ferry, \\u003cspan citationid=\\\"CR2\\\" class=\\\"CitationRef\\\"\\u003e1989\\u003c/span\\u003e; Enay \\u0026amp; Howarth, \\u003cspan citationid=\\\"CR13\\\" class=\\\"CitationRef\\\"\\u003e2019\\u003c/span\\u003e). The former lineage is represented in the studied interval of the uppermost Hypselocyclum Zone of the Submediterranean Province, from south-eastern France to central Poland, by the last smaller-sized forms of the genus \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e, both micro- and macroconchs (Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e). The final, somewhat isolated microconch member of that lineage is \\u0026ldquo;\\u003cem\\u003eOrthosphinctes\\u003c/em\\u003e (\\u003cem\\u003eArdescia\\u003c/em\\u003e)\\u0026rdquo; \\u003cem\\u003eperayensis\\u003c/em\\u003e Atrops. This form has been sometimes treated as the end-member of the separate \\u003cem\\u003eArdescia\\u003c/em\\u003e lineage (or even \\u003cem\\u003eLithacosphinctes\\u003c/em\\u003e lineage; see Moliner \\u0026amp; Ol\\u0026oacute;riz, \\u003cspan citationid=\\\"CR37\\\" class=\\\"CitationRef\\\"\\u003e2010\\u003c/span\\u003e), but it can be also considered as the final member of the small-sized \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e (\\u003cem\\u003eParataxioceras\\u003c/em\\u003e) \\u003cem\\u003eoppeli\\u003c/em\\u003e group, originated due to the heterochrony process. It may be concluded thus, it is possibly a small-sized form developed due to progenesis as shown by its ornamentation very similar to that of the inner whorls of its direct forerunner \\u0026ndash; the subspecies \\u003cem\\u003eA.\\u003c/em\\u003e (\\u003cem\\u003eP.\\u003c/em\\u003e) \\u003cem\\u003eoppeli parvum\\u003c/em\\u003e Atrops (see also Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e, p. 228, Fig.\\u0026nbsp;53).\\u003c/p\\u003e \\u003cp\\u003eWhen discussing the phylogenetical position of the genus \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e the most commonly interpretation given (Hantzpergue, \\u003cspan citationid=\\\"CR21\\\" class=\\\"CitationRef\\\"\\u003e1989\\u003c/span\\u003e; see also Enay et al., \\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e) suggested its origin from the Early Kimmeridgian \\u003cem\\u003eLithacosphinctes\\u003c/em\\u003e due to growth heterochrony \\u0026ndash; mostly progenesis and neoteny. The genus \\u003cem\\u003eLithacosphinctes\\u003c/em\\u003e as interpreted recently (e.g., Moliner \\u0026amp; Ol\\u0026oacute;riz, \\u003cspan citationid=\\\"CR37\\\" class=\\\"CitationRef\\\"\\u003e2010\\u003c/span\\u003e) includes both micro- and macroconchs corresponding to \\u0026ldquo;the most conservative lineage\\u0026rdquo; among the Early Kimmeridgian Submediterranean Ataxioceratinae: according to such interpretation the genus comprises also some evolute, smaller-sized microconch species occurring in the lower part of the Lothari Subzone, at the end of the lineage, and attributed previously to the \\u003cem\\u003eOrthosphinctes\\u003c/em\\u003e (\\u003cem\\u003eArdescia\\u003c/em\\u003e) \\u003cem\\u003einconditus\\u003c/em\\u003e group (see Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e), but excluding \\u0026ldquo;\\u003cem\\u003eO.\\u003c/em\\u003e (\\u003cem\\u003eA.\\u003c/em\\u003e)\\u0026rdquo; \\u003cem\\u003eperayensis\\u003c/em\\u003e as shown herein (see above). However, in accordance to that, there does not exist any link in the Submediterranean successions, both stratigraphical and morphological nature, between the older \\u003cem\\u003eLithacosphinctes\\u003c/em\\u003e group, and the younger well-developed \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e group. It is the reason that the proposed lineage of evolutionary development from the indigenous Submediterranean genus \\u003cem\\u003eLithacosphinctes\\u003c/em\\u003e to the suddenly appearing genus \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e is not accepted herein. It should be remembered that according to Moliner (\\u003cspan citationid=\\\"CR37\\\" class=\\\"CitationRef\\\"\\u003e2010\\u003c/span\\u003e), the genus \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e has been treated as descendent of a special group of the genus \\u003cem\\u003eArdescia\\u003c/em\\u003e (recognized as the separate genus, composed both of micro-and macroconchs), and moreover it was suggested that the genus \\u003cem\\u003eProgeronia\\u003c/em\\u003e evolved from \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e during the late Divisum Chron. Also that interpretation is not accepted because of the stratigraphical reasons \\u0026ndash; the occurrence of the typical representatives of the genus \\u003cem\\u003eProgeronia\\u003c/em\\u003e in much older deposits of the Early Kimmeridgian (see assemblage of unit A herein, see also e.g., Sarti, \\u003cspan citationid=\\\"CR41\\\" class=\\\"CitationRef\\\"\\u003e1993\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eThe new ammonite genera \\u0026ndash; \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eProgeronia\\u003c/em\\u003e which appeared during discussed transgression at the end of the Hypselocyclum Chron have had possibly their roots in the Mediterranean areas. Such an opinion was expressed already by Pavia et al. (\\u003cspan citationid=\\\"CR39\\\" class=\\\"CitationRef\\\"\\u003e1987\\u003c/span\\u003e) who suggested affinity of \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e to the Mediterranean Passendorferiinae, which interpretation has been, however, partly questioned by Enay et al. (\\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e). The Mediterranean origin of the discussed genera can be, however, additionally supported by the occurrence of the genera \\u003cem\\u003eProgeronia\\u003c/em\\u003e and possibly \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e deep in the Mediterranean Strombecki Zone \\u0026ndash; correlated with some lower parts of the Submediterranean Hypselocyclum Zone, markedly below the Lothari Subzone (see e.g., Sarti, \\u003cspan citationid=\\\"CR41\\\" class=\\\"CitationRef\\\"\\u003e1993\\u003c/span\\u003e). The principal reason for suggesting that representatives of the genera \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e and \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e have been originated from Mediterranean migrants is, however, that there are not known their earlier Submediterranean forerunners. Somewhat different situation is with the genus \\u003cem\\u003eProgeronia\\u003c/em\\u003e only, because there are known some forms occurring in older deposits of the Submediterranean succession which seem similar to typical representatives of the genus \\u0026ndash; e.g., such as \\u0026ldquo;\\u003cem\\u003eOrthoshinctes\\u003c/em\\u003e (\\u003cem\\u003eArdescia\\u003c/em\\u003e)\\u0026rdquo; \\u003cem\\u003eenayi\\u003c/em\\u003e Atrops occurring at the narrow interval between the lower and middle parts of the Platynota Zone from SE France to central Poland (Atrops, \\u003cspan citationid=\\\"CR1\\\" class=\\\"CitationRef\\\"\\u003e1982\\u003c/span\\u003e; see also Wierzbowski, \\u003cspan citationid=\\\"CR46\\\" class=\\\"CitationRef\\\"\\u003e2017\\u003c/span\\u003e). The open problem is, however, if they represent the fragmentarily recognized members of a single (?Mediterranean) lineage, or the local offshoots of Ataxioceratidae developed during the transgressive episodes. A generally poor knowledge on details of the succession (and their precise dating) yielding ammonites referred to as \\u003cem\\u003eOrthosphinctes, Crussoliceras\\u003c/em\\u003e and \\u003cem\\u003eProgeronia\\u003c/em\\u003e (e.g., Pavia et al., \\u003cspan citationid=\\\"CR39\\\" class=\\\"CitationRef\\\"\\u003e1987\\u003c/span\\u003e; Sarti, \\u003cspan citationid=\\\"CR41\\\" class=\\\"CitationRef\\\"\\u003e1993\\u003c/span\\u003e) in the crucial intervals of the Lower Kimmeridgian (mostly the Strombecki Zone) in the Mediterranean sections prevents the detailed recognition of the evolutionary development of the discussed lineages.\\u003c/p\\u003e \\u003cp\\u003eThe evolutionary development of ammonites of the family Aulacostephanidae proceeded a different way. In central Poland, in the area of Burzenin, north-west of the Holy Cross Mountains, in the deposits of open-marine environment of the middle part of the Hypselocyclum Zone (i.e. older than studied herein), was noted a marked increase in number, and in morphological development of representatives of the family (Wierzbowski, \\u003cspan citationid=\\\"CR46\\\" class=\\\"CitationRef\\\"\\u003e2017\\u003c/span\\u003e). These ammonites belonged here to two different groups: that showing a more heavily-ribbed shells and representing possibly a more shallow-water environment such as \\u003cem\\u003eEurasenia\\u003c/em\\u003e and \\u003cem\\u003eInvoluticeras\\u003c/em\\u003e, and another one composed of \\u003cem\\u003eVineta\\u003c/em\\u003e to \\u003cem\\u003eBalticeras\\u003c/em\\u003e and the first \\u003cem\\u003eRasenioides\\u003c/em\\u003e showing more subdued ribbing, exploring possibly more-open marine, nektonic environment (Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e). The overall transgression at the end of the Hypselocyclum Chron brought the heavily-ribbed Aulacostephanidae into flooded area of the shallow-water carbonate platform of the Holy Cross Mountains. Their share within the whole ammonite fauna of unit A in the Małogoszcz section ranges even up to about 35%. On the other hand, the aulacostephanids of the second group were totally absent in this area.\\u003c/p\\u003e \\u003cp\\u003eSimilar features of distribution of ammonites of the family Aulacostephanidae have been observed also in other shallow-water areas of the Western European Shelf, corresponding to the so-called \\u0026ldquo;Western European Swell\\u0026rdquo; (Hantzpergue, \\u003cspan citationid=\\\"CR21\\\" class=\\\"CitationRef\\\"\\u003e1989\\u003c/span\\u003e; Hantzpergue et al., \\u003cspan citationid=\\\"CR23\\\" class=\\\"CitationRef\\\"\\u003e1997\\u003c/span\\u003e; see also Enay et al., \\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e). A sudden appearance of ammonites of the genus \\u003cem\\u003eEurasenia\\u003c/em\\u003e, along and above the occurrence of \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e of \\u003cem\\u003eA. lothari\\u003c/em\\u003e group, \\u0026ldquo;coincided with a maximum sea-level rise\\u0026rdquo; (Hantzpergue, \\u003cspan citationid=\\\"CR22\\\" class=\\\"CitationRef\\\"\\u003e1995\\u003c/span\\u003e, p. 247). The horizons \\u003cem\\u003eaulsnisa\\u003c/em\\u003e and \\u003cem\\u003emanicata\\u003c/em\\u003e as defined on the basis of \\u003cem\\u003eEurasenia\\u003c/em\\u003e in the Western European Shelf can be just correlated with the \\u003cem\\u003esemistriatum\\u003c/em\\u003e horizon of the upper part of the Hypselocyclum Zone of the Submediterranean zonation (Hantzpergue, \\u003cspan citationid=\\\"CR21\\\" class=\\\"CitationRef\\\"\\u003e1989\\u003c/span\\u003e; Matyja \\u0026amp; Wierzbowski, \\u003cspan citationid=\\\"CR33\\\" class=\\\"CitationRef\\\"\\u003e2000\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eOn the other hand, a sudden development of the genus \\u003cem\\u003eRasenioides\\u003c/em\\u003e representing the second group of Aulacostephanidae took place in the areas of northern and north-western Europe corresponding to the Subboreal Province, or representing the transitional areas between Submediterranean and Subboreal provinces. The dominance of these ammonites is observed e.g., in England (Birkelund et al., \\u003cspan citationid=\\\"CR5\\\" class=\\\"CitationRef\\\"\\u003e1983\\u003c/span\\u003e), where their appearance defines the base of the Askepta Subzone correlated with the upper part of the Subboreal Cymodoce Zone, but also in a similar stratigraphical position in the Peri-Baltic Syneclise from the north-eastern Poland to Lithuania (e.g., Wierzbowski et al., \\u003cspan citationid=\\\"CR50\\\" class=\\\"CitationRef\\\"\\u003e2015\\u003c/span\\u003e). In Aquitaine (Hantzpergue, \\u003cspan citationid=\\\"CR21\\\" class=\\\"CitationRef\\\"\\u003e1989\\u003c/span\\u003e; Hantzpergue et al., \\u003cspan citationid=\\\"CR23\\\" class=\\\"CitationRef\\\"\\u003e1997\\u003c/span\\u003e), the appearance of \\u003cem\\u003eRasenioides\\u003c/em\\u003e defines the base of the \\u003cem\\u003easkeptus\\u003c/em\\u003e horizon within the Chatelaillonensis Subzone \\u0026ndash; which is located directly above the \\u003cem\\u003eaulsnisa-manicata\\u003c/em\\u003e horizons with \\u003cem\\u003eEurasenia.\\u003c/em\\u003e The crucial for correlation of the discussed aulacostephanid (Subboreal) and the ataxioceratid (Submediterranean) zonations appeared the data from boreholes in the Zalesie Anticline in northern Poland studied by the present author. The recognized here (Matyja \\u0026amp; Wierzbowski, \\u003cspan citationid=\\\"CR33\\\" class=\\\"CitationRef\\\"\\u003e2000\\u003c/span\\u003e, Figs.\\u0026nbsp;\\u003cspan refid=\\\"Fig3\\\" class=\\\"InternalRef\\\"\\u003e3\\u003c/span\\u003e\\u0026ndash;\\u003cspan refid=\\\"Fig4\\\" class=\\\"InternalRef\\\"\\u003e4\\u003c/span\\u003e) nearly coeval occurrence of early \\u003cem\\u003eRasenioides\\u003c/em\\u003e and \\u0026ldquo;\\u003cem\\u003eOrthosphinctes\\u003c/em\\u003e (\\u003cem\\u003eArdescia\\u003c/em\\u003e)\\u0026rdquo; \\u003cem\\u003eperayensis\\u003c/em\\u003e Atrops indicates, the correlation of the lowermost part of the Askepta Subzone or \\u003cem\\u003easkeptus\\u003c/em\\u003e horizon of the Chatelaillonensis Subzone in Subboreal or transitional areas of the northern Europe with the \\u003cem\\u003eperayensis\\u003c/em\\u003e horizon of the uppermost part of the Hypselocylum Zone of the Submediterranean Province. It should be remembered, however, that the occurrence of \\u0026ldquo;\\u003cem\\u003eO.\\u003c/em\\u003e(\\u003cem\\u003eA.\\u003c/em\\u003e)\\u0026rdquo; \\u003cem\\u003eperayensis\\u003c/em\\u003e along with late representatives of the genus \\u003cem\\u003eRasenioides\\u003c/em\\u003e transitional to \\u003cem\\u003eAulacostephanoides\\u003c/em\\u003e, as reported in archival materials from core Kcynia IG-IV in northern Poland (Matyja \\u0026amp; Wierzbowski, \\u003cspan citationid=\\\"CR33\\\" class=\\\"CitationRef\\\"\\u003e2000\\u003c/span\\u003e, Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig2\\\" class=\\\"InternalRef\\\"\\u003e2\\u003c/span\\u003e), suggests also a local higher upward range of that species. Anyway, the sudden invasion of the the Subboreal \\u003cem\\u003eRasenioides\\u003c/em\\u003e to the north, coincided possibly in time with a sudden spread across the Submediterranean Province of ammonites of the Mesogean affinity \\u0026ndash; such as \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, G\\u003cem\\u003earnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eProgeronia\\u003c/em\\u003e, as discussed above.\\u003c/p\\u003e \\u003cp\\u003eUnit B in the Małogoszcz section has clearly the regressive character as indicated by its lithological characteristics (see above). The assemblage of ammonites consists mostly of Ataxioceratidae (\\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eProgeronia\\u003c/em\\u003e) and to lesser degree of the heavily-ribbed Aulacostephanidae (\\u003cem\\u003eEurasenia\\u003c/em\\u003e, \\u003cem\\u003eProrasenia\\u003c/em\\u003e, rare \\u003cem\\u003eRasenia\\u003c/em\\u003e), showing thus a marked similarity to that of unit A, but without \\u003cem\\u003eAtaxioceras.\\u003c/em\\u003e The younger ammonite assemblage of unit C reveals, however, a markedly different character.\\u003c/p\\u003e \\u003cp\\u003eThe most important new faunal elements in ammonite assemblage of unit C are the suddenly appearing fairly numerous Aspidoceratidae, especially those of the genus \\u003cem\\u003ePseudhimalayites\\u003c/em\\u003e with the species \\u003cem\\u003eP. uhlandi\\u003c/em\\u003e (Oppel). The roots of the genus were possibly in the Western Tethyan areas, or even far outside, thus a wide distribution of this genus in many European sections was an effect of migration (see e.g., Schweigert, \\u003cspan citationid=\\\"CR43\\\" class=\\\"CitationRef\\\"\\u003e1997\\u003c/span\\u003e). The species \\u003cem\\u003eP. uhlandi\\u003c/em\\u003e associated with many other Tethyan ammonites, such as various species of \\u003cem\\u003eNebrodites\\u003c/em\\u003e, occurs commonly in the Western Tethyan areas, and their foreland \\u0026ndash; in the Submediterranean Province, defining everywhere the upper part of the Divisum Zone or of the Herbichi Zone \\u0026ndash; the Uhlandi Subzone (e.g., Geyer, \\u003cspan citationid=\\\"CR18\\\" class=\\\"CitationRef\\\"\\u003e1961\\u003c/span\\u003e, Sarti, \\u003cspan citationid=\\\"CR41\\\" class=\\\"CitationRef\\\"\\u003e1993\\u003c/span\\u003e; Caracuel et al., \\u003cspan citationid=\\\"CR9\\\" class=\\\"CitationRef\\\"\\u003e1998\\u003c/span\\u003e). Even in the studied Submediterranean succession at Małogoszcz \\u0026ndash; some representatives of various species of \\u003cem\\u003eNebrodites\\u003c/em\\u003e have been encountered along with \\u003cem\\u003eP. uhlandi\\u003c/em\\u003e in unit C. Additionally, the not numerous Aulacostephanidae are markedly impoverished here, both in number and in presence of heavily-ribbed forms. All these data strongly suggests a transgressive character of unit C. It should be remembered that the deposits of the Uhlandi Subzone are treated as transgressive in character in many areas of Europe (e.g., Marques \\u0026amp; Ol\\u0026oacute;riz, \\u003cspan citationid=\\\"CR31\\\" class=\\\"CitationRef\\\"\\u003e1992\\u003c/span\\u003e). This high sea-level can be correlated possibly with the minimum of 100-kyr eccentricity cycle (see Boulila et al., \\u003cspan citationid=\\\"CR6\\\" class=\\\"CitationRef\\\"\\u003e2008\\u003c/span\\u003e, \\u003cspan citationid=\\\"CR7\\\" class=\\\"CitationRef\\\"\\u003e2010\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eUnits D and E in the Małogoszcz section yielded numerous specimens of \\u003cem\\u003ePseudhimalayites uhlandi\\u003c/em\\u003e (Oppel). Unfortunately the distribution of these specimens in the succession cannot be traced in details mostly because of lack of precise location of the particular finds. It is only the topmost part of unit E recognized which shows a marked concentration of the \\u003cem\\u003ePseudhimalayites\\u003c/em\\u003e shells, some of them attaining large sizes. In a similar stratigraphical position has been found also a few specimens of Phylloceratidae of giant sizes (about 0.5 m in diameter), interpreted herein as the allochtonous elements which appearance has been possibly related to the post-mortem drift of shells from the Tethyan areas (thus not taken into account in the diagram of distribution of the ammonite genera in the succession \\u0026ndash; see Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig2\\\" class=\\\"InternalRef\\\"\\u003e2\\u003c/span\\u003e). It seems highly probable that the concentration of all these shells at the top of unit E resulted from a very high sea-level. This may correspond to the minimum of the next 100-kyr eccentricity cycle well documented in the late Divisum Subchron (see Boulila et al., \\u003cspan citationid=\\\"CR6\\\" class=\\\"CitationRef\\\"\\u003e2008\\u003c/span\\u003e, \\u003cspan citationid=\\\"CR7\\\" class=\\\"CitationRef\\\"\\u003e2010\\u003c/span\\u003e). This level corresponds possibly also to the \\u003cem\\u003ebalderum\\u003c/em\\u003e horizon (or subzone) as marked by common occurrence of the Tethyan form \\u003cem\\u003eIdoceras balderum\\u003c/em\\u003e (Oppel) well documented at the top of the Uhlandi Subzone of the Divisum Zone in the Submediterranean areas of southern Germany to south-eastern France (see e.g., Hantzpergue et al., \\u003cspan citationid=\\\"CR23\\\" class=\\\"CitationRef\\\"\\u003e1997\\u003c/span\\u003e). Such stratigraphical interpretation can be also confirm by finding in the Małogoszcz section, at the top of unit E, of a single specimen of \\u003cem\\u003eTaramelliceras\\u003c/em\\u003e (\\u003cem\\u003eTaramelliceras\\u003c/em\\u003e) \\u003cem\\u003ecompsum\\u003c/em\\u003e (Oppel) of the Tethyan origin.\\u003c/p\\u003e \\u003cp\\u003eSome changes in ammonites of the family Ataxioceratidae seen already in unit C, recognized also in units D-E include the emerging of the new genus \\u003cem\\u003eTolvericeras.\\u003c/em\\u003e The genus as interpreted by Enay et al. (\\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e) derived possibly from \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eCrussoliceras.\\u003c/em\\u003e The rare specimens discovered in the Małogoszcz succession show a marked similarity to \\u0026ldquo; \\u003cem\\u003eTolvericeras\\u003c/em\\u003e n. sp.\\u0026rdquo; in Gygi (\\u003cspan citationid=\\\"CR19\\\" class=\\\"CitationRef\\\"\\u003e2003\\u003c/span\\u003e, p. 144, Figs.\\u0026nbsp;165\\u0026ndash;166) coming from the Divisum Zone of northern Switzerland, showing independently some similarity to \\u003cem\\u003eGarnierisphinctes.\\u003c/em\\u003e On the other hand, the units C-D-E yielded also numerous specimens of \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e [\\u003cem\\u003eC.\\u003c/em\\u003e cf. \\u003cem\\u003ecrusoliense\\u003c/em\\u003e (Font.)], \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e [\\u003cem\\u003eG. plebejus\\u003c/em\\u003e (Neumayr and \\u003cem\\u003eG. championneti\\u003c/em\\u003e (Neum., \\u003cem\\u003eG. semigarnieri\\u003c/em\\u003e (Geyer] and less common \\u003cem\\u003eProgeronia\\u003c/em\\u003e [ \\u003cem\\u003eP.\\u003c/em\\u003e (\\u003cem\\u003eP.\\u003c/em\\u003e) \\u003cem\\u003eeggeri\\u003c/em\\u003e (von Ammon), \\u003cem\\u003eP.\\u003c/em\\u003e (\\u003cem\\u003eH.\\u003c/em\\u003e) \\u003cem\\u003ebreviceps\\u003c/em\\u003e (Quenstedt)].\\u003c/p\\u003e \\u003cp\\u003eThe recognized changes within family Aulacostephanidae in units D-E of the Małogoszcz section include especially the rare occurrences of the advanced morphologically representatives of the genus \\u003cem\\u003eRasenioides\\u003c/em\\u003e, such as \\u003cem\\u003eR. moeschi\\u003c/em\\u003e (Oppel). Their appearance, already at the base of unit D, can be treated as a manifestation of \\u0026ldquo;southern drift\\u0026rdquo; of the genus which developed earlier in the Subboreal Province (see Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e; see also comments above): this phenomenon resulted possibly from appearance in the succession studied of marly facies resembling the \\u0026ldquo;Virgulian Facies\\u0026rdquo; of north-western Europe suitable for development of the Subboreal fauna (cf. Hantzpergue, \\u003cspan citationid=\\\"CR22\\\" class=\\\"CitationRef\\\"\\u003e1995\\u003c/span\\u003e). On the other hand, the local occurrence of a special group of aulacostephanids intermediate between some \\u003cem\\u003eEurasenia\\u003c/em\\u003e and \\u003cem\\u003ePararasenia\\u003c/em\\u003e has been recognized in upper parts of unit E. They show heavy ornamentation on the whorl side characteristic of both \\u003cem\\u003eEurasenia\\u003c/em\\u003e and \\u003cem\\u003ePararasenia\\u003c/em\\u003e, but reveal an incipient obliteration of ribbing in the ventral side of whorls typical of the genus \\u003cem\\u003ePararasenia.\\u003c/em\\u003e The specimen (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003ec-d) studied resembles the heavily ribbed species \\u003cem\\u003ePararasenia quenstedti\\u003c/em\\u003e Durand (cf. Ziegler, \\u003cspan citationid=\\\"CR53\\\" class=\\\"CitationRef\\\"\\u003e1962\\u003c/span\\u003e) reported in younger beds of the earliest Late Kimmeridgian in the Małogoszcz section (Kutek, \\u003cspan citationid=\\\"CR27\\\" class=\\\"CitationRef\\\"\\u003e1968\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eTwo specimens coming from units B and D-E (Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig7\\\" class=\\\"InternalRef\\\"\\u003e7\\u003c/span\\u003ea-b) are representatives of NW European Subboreal genus \\u003cem\\u003eRasenia.\\u003c/em\\u003e They show a weakly involute to weakly evolute coiling, rather distant primary ribs, and a high number of secondary ribs (the secondary/primary rib ratio equals 5.0 at about 50 mm diameter). The specimens belong to \\u003cem\\u003eRasenia involuta\\u003c/em\\u003e Spath, a very characteristic species commonly encountered in southern England where the specimens coming from (e.g., Birkelund et al., \\u003cspan citationid=\\\"CR5\\\" class=\\\"CitationRef\\\"\\u003e1983\\u003c/span\\u003e, Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig3\\\" class=\\\"InternalRef\\\"\\u003e3\\u003c/span\\u003eA-D) are very similar to the specimens studied. It is worth noting that all these specimens resemble also the heavily-ribbed form referred to as \\u003cem\\u003eRasenioides ecolisnus\\u003c/em\\u003e (Hantzpergue, \\u003cspan citationid=\\\"CR21\\\" class=\\\"CitationRef\\\"\\u003e1989\\u003c/span\\u003e, pl. 35: c-f). It should be remembered that the latter is treated as a form which begins a side branch of the \\u003cem\\u003eRasenioides\\u003c/em\\u003e lineage, leading in its evolutionary development to origin of a more heavily-ribbed forms of the genus \\u003cem\\u003eAulacostephanoides\\u003c/em\\u003e (Hantzpergue, \\u003cspan citationid=\\\"CR21\\\" class=\\\"CitationRef\\\"\\u003e1989\\u003c/span\\u003e, Figs.\\u0026nbsp;130,133), or marking the transition to the genus \\u003cem\\u003eAulacostephanus\\u003c/em\\u003e (Borreli, \\u003cspan citationid=\\\"CR8\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e, Fig.\\u0026nbsp;\\u003cspan refid=\\\"Fig2\\\" class=\\\"InternalRef\\\"\\u003e2\\u003c/span\\u003e). The possible phylogenetical link between late \\u003cem\\u003eRasenia involuta\\u003c/em\\u003e, and some early forms of \\u003cem\\u003eAulacostephanoides/Aulacostephanus\\u003c/em\\u003e (as suggested herein) can be thus considered as an alternative proposal for the lineage (assuming the phylogenetical affinity between \\u003cem\\u003eR. involuta\\u003c/em\\u003e and \\u003cem\\u003eR. ecolisnus\\u003c/em\\u003e), which developed independently of that leading from the densely-ribbed \\u003cem\\u003eRasenioides\\u003c/em\\u003e to the typical \\u003cem\\u003eAulacostephanoides\\u003c/em\\u003e (cf. Borreli, \\u003cspan citationid=\\\"CR8\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e).\\u003c/p\\u003e \\u003c/div\\u003e\"},{\"header\":\"General comments\",\"content\":\"\\u003cp\\u003eThe late Early Kimmeridgian corresponding to the late Hypselocyclum and Divisum chrons (or to the late Cymodoce Chron) was a fairly short time (about 260 to 300 kyr) when the diversity in development of many ammonites lineages changed markedly. This phylogenetical turnover resulted in origination and termination of several lineages, and has been strictly controlled by changes in the environment, generally in progress of the overall transgression, which occurred especially along the northern Tethyan Shelf in the wide areas of Submediterranean to Subboreal provinces of Europe. The transgression was strictly controlled by syn-sedimentary tectonic activity, and additionally superimposed transgressive pulses corresponding to climate changes, related mostly with orbitally-controlled cyclicity. The studied Submediterranean succession at Małogoszcz in the south-western margin of the Holy Cross Mountains, central Poland was formed in changing water depth \\u0026ndash; from initial transgression flooding the shallow-water carbonate platform to a fairly deep water environment, which showed similarity to that of the \\u0026ldquo;Virgulian Facies\\u0026rdquo; of north-western Europe. The development of the coeval deeper-water sedimentation is recognized widely in Submediterranean areas from central Poland to south-eastern France and Spain, being everywhere strictly correlated to the marked evolutionary transformations of the ammonite faunas: their migrations, decline or radiation.\\u003c/p\\u003e \\u003cp\\u003eThe beginning of the marine transgression already at the end of the Hypselocyclum Chron brought into the whole discussed areas of Submediterranean Europe the new ataxioceratid ammonites including closely related genera \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eProgeronia\\u003c/em\\u003e having possibly their roots in the Mediterranean Tethys. The development of these ammonites was strictly related to changes of the environmental conditions into those compatible with their physiological tolerance, which also affected the group of older indigenous Ataxioceratinae, such as \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e, \\u003cem\\u003eOrthosphinctes\\u003c/em\\u003e and \\u003cem\\u003eArdescia\\u003c/em\\u003e, and resulted in its total decline. On the other hand, the changes in environment strongly disturbed also the development of other groups of ammonites, mostly Aulacostephanidae: some of them, especially the heavily- ribbed forms (\\u003cem\\u003eEurasenia\\u003c/em\\u003e, \\u003cem\\u003eInvoluticeras\\u003c/em\\u003e) fluorished on the flooded areas of the carbonate platform like that of the Holy Cross Mts., some other like the more open-marine \\u003cem\\u003eRasenioides\\u003c/em\\u003e migrated toward the north into a deeper-water environment of Subboreal Province. The progress of the transgression brought onto the Tethyan Shelf (but also into the Mediterranean Tethys) during the late Divisum Chron also other ammonites \\u0026ndash; mostly Aspidoceratidae, especially of the genus \\u003cem\\u003ePseudhimalayites.\\u003c/em\\u003e\\u003c/p\\u003e \\u003cp\\u003eThe taxonomic diversity within \\u003cem\\u003eCrussoliceras-Garnierisphinctes-Progeronia\\u003c/em\\u003e faunas increases upwards in the succession studied at Małogoszcz. This is shown by the appearance of larger number of species, but also by the evolutionary development of the new genus \\u003cem\\u003eTolvericeras\\u003c/em\\u003e showing affinity to \\u003cem\\u003eGarnierisphinctes.\\u003c/em\\u003e It is in general accordance with observation of Enay et al. (\\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e) who suggested the evolutionary path from \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e to restricted group of species placed around the type species of \\u003cem\\u003eTolvericeras\\u003c/em\\u003e already during the late Divisum Chron, at the end of Early Kimmeridgian, in the Submediterranean Province in SE France and Switzerland. Later on, \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e and \\u003cem\\u003eTolvericeras\\u003c/em\\u003e were rather not commonly encountered here, occurring mostly during the Late Kimmeridgian in the Western European Swell \\u0026ndash; the transitional area between Submediterranean and Subboreal provinces, where also some forms close to \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e evolved at the end of the Kimmeridgian into \\u003cem\\u003ePseudogravesia\\u003c/em\\u003e to \\u003cem\\u003eGravesia\\u003c/em\\u003e group (Enay et al., \\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e; cf. also Hantzpergue et al., 1989). On the other hand, a more common occurrence of \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e and \\u003cem\\u003eTolvericeras\\u003c/em\\u003e during the Late Kimmeridgian has been recognized in the Subboreal Province in England: the appearance there of \\u003cem\\u003eSubdichotomites\\u003c/em\\u003e, which possibly evolved from \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e at the end of the Kimmeridgian, gave subsequently rise to the Boreal Dorsoplanitinae (Enay et al., \\u003cspan citationid=\\\"CR14\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eThe evolutionary development of Aulacostephanidae at the end of the Early Kimmeridgian \\u0026ndash; beginning of the Late Kimmeridgian in Europe has been the subject of fairly diversified interpretations. This is mostly because of the incompleteness of the fossil records, at least partly resulting from marked changes of palaeobiogeographical ranges of these ammonites in time. The only indigenous lineage traced in the Holy Cross Mts. area is that leading from the heavily-ribbed \\u003cem\\u003eEurasenia\\u003c/em\\u003e, like \\u003cem\\u003eE. pendula\\u003c/em\\u003e and \\u003cem\\u003eE. trifurcata\\u003c/em\\u003e recorded in the succession studied, to \\u003cem\\u003ePararasenia\\u003c/em\\u003e which shows the smooth band in the ventral side of whorls (Ziegler, \\u003cspan citationid=\\\"CR53\\\" class=\\\"CitationRef\\\"\\u003e1962\\u003c/span\\u003e; see also Wierzbowski, \\u003cspan citationid=\\\"CR48\\\" class=\\\"CitationRef\\\"\\u003e2022\\u003c/span\\u003e). Another lineage, already discussed above, originated from the weakly-ornamented \\u003cem\\u003eVineta\\u003c/em\\u003e to \\u003cem\\u003eRasenioides\\u003c/em\\u003e, but its further development included migration of younger forms of the lineage towards the north where they gave rise to early \\u003cem\\u003eAulacostephanoides.\\u003c/em\\u003e Even more nebulous is the development of the third lineage of aulacostephanids. This possibly included at its base some moderately involute and heavily-ribbed \\u003cem\\u003eRasenia\\u003c/em\\u003e (like \\u003cem\\u003eR. involuta\\u003c/em\\u003e and possibly similarly looking \\u0026ldquo;\\u003cem\\u003eRasenioides\\u003c/em\\u003e\\u0026rdquo; \\u003cem\\u003eecolisnus\\u003c/em\\u003e, as discussed above). They seem to intergrade even with the \\u0026ldquo;transitional\\u0026rdquo; genus \\u003cem\\u003eZonovia\\u003c/em\\u003e showing some weakening of the ribbing on the ventral side of outer whorls (see Birkelund et al., \\u003cspan citationid=\\\"CR4\\\" class=\\\"CitationRef\\\"\\u003e1978\\u003c/span\\u003e). The lineage may continue into some more heavily-ribbed early Late Kimmeridgian aulacostephanids referred in older classifications to as \\u003cem\\u003eAulacostephanoides\\u003c/em\\u003e, and more recently correlated with \\u003cem\\u003eAulacostephanus\\u003c/em\\u003e (Borreli, \\u003cspan citationid=\\\"CR8\\\" class=\\\"CitationRef\\\"\\u003e2014\\u003c/span\\u003e).\\u003c/p\\u003e \\u003cp\\u003eThe changes in distribution of ammonites were accompanied by important development in their evolution. Such a drastic example of overlapping of ranges of distribution of the ammonite faunas belonging to different lineages and representing the various stages of their evolutionary development has been reported in the successions of central and southern parts of the Russian Platform, especially Tatarstan, central European Russia (see Rogov et al., \\u003cspan citationid=\\\"CR40\\\" class=\\\"CitationRef\\\"\\u003e2017\\u003c/span\\u003e). The recognized there a narrow stratigraphical horizon with Submediterranean \\u003cem\\u003eCrussoliceras atavum\\u003c/em\\u003e (Schneid) - \\u003cem\\u003eC. lacertosum\\u003c/em\\u003e (Fonatnnes), possibly corresponds only to some upper parts of the Divisum Zone, and it is underlain by beds with Subboreal \\u003cem\\u003eRasenia\\u003c/em\\u003e and \\u003cem\\u003eZonovia\\u003c/em\\u003e, and overlain by beds with \\u003cem\\u003eRasenioides\\u003c/em\\u003e, all of them belonging to the upper part of the Cymodoce Zone \\u0026ndash; the Askepta Subzone. Additionally, the occasional occurrence of the Boreal ammonites of the genus \\u003cem\\u003eAmoebites\\u003c/em\\u003e, transitional already to younger \\u003cem\\u003eEuprionoceras\\u003c/em\\u003e, indicates the evolutionary changes in the cardioceratid lineage during the late Kitchini Chron.\\u003c/p\\u003e \\u003cp\\u003eThe problems of general classification of the Late Kimmeridgian ammonites attributed to the genus \\u003cem\\u003eAulacostephanus\\u003c/em\\u003e is generally outside the scope of the present study. It is only the genus \\u003cem\\u003eZenostephanus\\u003c/em\\u003e (formerly \\u003cem\\u003eXenostephanus\\u003c/em\\u003e) which evolutionary development is partly related to those of some discussed here aulacostephanids, and which represents a similar stratigraphical range. The genus evolved probably from the Subboreal \\u003cem\\u003eRasenia evoluta\\u003c/em\\u003e, as evidenced by occurrence of the intermediate forms already at the end of the Cymodoce Chron in southern England (Birkelund et al., \\u003cspan citationid=\\\"CR5\\\" class=\\\"CitationRef\\\"\\u003e1983\\u003c/span\\u003e). These migrated successively into the Arctic areas of the Boreal Province at the boundary between the Early and Late Kimmeridgian as a consequence of a large transgression giving then the onset to the new lineage (e.g., Wierzbowski \\u0026amp; Smelror, \\u003cspan citationid=\\\"CR49\\\" class=\\\"CitationRef\\\"\\u003e2020\\u003c/span\\u003e), but appeared soon thereafter as representatives of the fully developed genus \\u003cem\\u003eZenostephanus\\u003c/em\\u003e in north-eastern Europe in areas of the Russian Sea (Rogov et al., \\u003cspan citationid=\\\"CR40\\\" class=\\\"CitationRef\\\"\\u003e2017\\u003c/span\\u003e). The genus can be considered as a possible forerunner of a group of the Late Kimmeridgian \\u003cem\\u003eAulacostephanus\\u003c/em\\u003e, widely distributed in NW, central, and NE European areas, as already suggested by Birkelund \\u0026amp; Callomon (\\u003cspan citationid=\\\"CR3\\\" class=\\\"CitationRef\\\"\\u003e1985\\u003c/span\\u003e), which assumption has a large consequences for interpretation of the phylogenetical pattern of development of Aulacostephanidae.\\u003c/p\\u003e\"},{\"header\":\"Declarations\",\"content\":\"\\u003cp\\u003eAchnowledgements: The study was financed by the Polish National Science Center (project no 2020/39/B/ST10/01489). Special thanks are to Błażej Błażejowski for his help in preparation of photographs of ammonites, and to Hubert Wierzbowski for fruitful discussion.\\u003c/p\\u003e\\u003ch2\\u003eConflict of interest:\\u003c/h2\\u003e \\u003cp\\u003eThe author declares no conflicts of interest.\\u003c/p\\u003e \\u003c/p\\u003e\"},{\"header\":\"References\",\"content\":\"\\u003col\\u003e\\u003cli\\u003e\\u003cspan\\u003eAtrops, F. (1982). Le sous-family des Ataxioceratinae (Ammonitina) dans le Kimm\\u0026eacute;ridgien inf\\u0026eacute;rieur du Sud-Est de la France. Syst\\u0026eacute;matique, evolution, chronostratigraphie des genres. \\u003cem\\u003eOrthosphinctes et Ataxioceras Documents des Laboratoires de G\\u0026eacute;ologie de Lyon\\u003c/em\\u003e, \\u003cem\\u003e83\\u003c/em\\u003e, 1\\u0026ndash;463.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eAtrops, F., \\u0026amp; Ferry, S. (1989). Sequence stratigraphy and changes in the ammonite faunas (Upper Jurassic, S-E France). In: \\u003cem\\u003e2\\u0026egrave;me Congres Fran\\u0026ccedil;ais de Sedimentologie. Mesozoic Eustasy Record on Western Tethyan Margin\\u003c/em\\u003e (pp. 7\\u0026ndash;9). Lyon.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eBirkelund, T., \\u0026amp; Callomon, J. H. (1985). The Kimmeridgian ammonite fauns of Milne Land, central East Greenland. \\u003cem\\u003eGr\\u0026oslash;nlands Geologiske Unders\\u0026oslash;gelse\\u003c/em\\u003e, \\u003cem\\u003e153\\u003c/em\\u003e, 1\\u0026ndash;56.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eBirkelund, T., Thusu, B., \\u0026amp; Vigran, J. (1978). Jurassic-Cretaceous biostratigraphy of Norway, with comments on the British \\u003cem\\u003eRasenia cymodoce\\u003c/em\\u003e Zone. \\u003cem\\u003ePalaeontology\\u003c/em\\u003e, \\u003cem\\u003e21\\u003c/em\\u003e(1), 31\\u0026ndash;63.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eBirkelund, T., Callomon, J. H., Clausen, C. K., N\\u0026oslash;hr Hansen, H., \\u0026amp; Salinas, I. (1983). The Lower Kimmeridgian Clay at Westbury, Wiltshire, England. \\u003cem\\u003eProceedings of Geologists\\u0026rsquo; Association, 94\\u003c/em\\u003e (4), 289\\u0026ndash;309.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eBoulila, S., Galbrun, B., Hinnov, L. A., \\u0026amp; Collin, P. Y. (2008). 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Updated biostratigraphy of Jurassic (lower Kimmeridgian) deposits containing the ammonite \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e from the eastern Iberian Range, northeastern Spain. \\u003cem\\u003eGFF\\u003c/em\\u003e, \\u003cem\\u003e131\\u003c/em\\u003e, 193\\u0026ndash;203.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eMoliner, L., \\u0026amp; Ol\\u0026oacute;riz, F. (2010). New Lower Kimmeridgian ataxioceratin ammonite from the eastern Iberian Chain, Spain: Systematic, biogeographic, and biostratigraphic relevance. \\u003cem\\u003eActa Palaeontologica Polonica\\u003c/em\\u003e, \\u003cem\\u003e55\\u003c/em\\u003e(1), 99\\u0026ndash;110.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eOl\\u0026oacute;riz, F. (1978). Kimmeridgiense-Tithonico inferior en el sector central de las Cordilleras Beticas (Zona Subbetica). Paleontologia. 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The Oxfordian and Lower Kimmeridgian of the Peri-Baltic Syneclise (north-eastern Poland: stratigraphy, ammonites, microfossils (foraminifers, radiolarians), facies and palaeogeographical implications. \\u003cem\\u003eNeues Jahrbuch fȕr Geologie und Pal\\u0026auml;ontologie\\u003c/em\\u003e, \\u003cem\\u003e277\\u003c/em\\u003e(1), 63\\u0026ndash;104. \\u003cspan class=\\\"ExternalRef\\\"\\u003e\\u003cspan class=\\\"RefSource\\\"\\u003e10.1127/njgpa/2015/0496)\\u003c/span\\u003e\\u003cspan address=\\\"10.1127/njgpa/2015/0496)\\\" targettype=\\\"DOI\\\" class=\\\"RefTarget\\\"\\u003e\\u003c/span\\u003e\\u003c/span\\u003e.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eWierzbowski, H. (2019). Palaeoenvironmental changes recorded in oxygen and carbon isotope composition of Kimmeridgian (Upper Jurassic) carbonates from central Poland. \\u003cem\\u003eGeological Quarterly\\u003c/em\\u003e, \\u003cem\\u003e63\\u003c/em\\u003e(2), 259\\u0026ndash;274. \\u003cspan class=\\\"ExternalRef\\\"\\u003e\\u003cspan class=\\\"RefSource\\\"\\u003ehttp://dx.doi.org/10.7306/gq.1471)\\u003c/span\\u003e\\u003cspan address=\\\"10.7306/gq.1471)\\\" targettype=\\\"DOI\\\" class=\\\"RefTarget\\\"\\u003e\\u003c/span\\u003e\\u003c/span\\u003e.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eZiegler, B. (1979). Idoceras und verwandte Ammoniten_Gattungen im Oberjura Schwabens. \\u003cem\\u003eEclogae Geologicae Helvetiae\\u003c/em\\u003e, \\u003cem\\u003e52\\u003c/em\\u003e(1), 19\\u0026ndash;56.\\u003c/span\\u003e\\u003c/li\\u003e \\u003cli\\u003e\\u003cspan\\u003eZiegler, B. (1962). Die Ammoniten Gattung \\u003cem\\u003eAulacostephanus\\u003c/em\\u003e im Oberjura (Taxonomie, Stratigraphie, Biologie). \\u003cem\\u003ePalaeontographica\\u003c/em\\u003e, \\u003cem\\u003e119A\\u003c/em\\u003e, 1\\u0026ndash;172.\\u003c/span\\u003e\\u003c/li\\u003e \\u003c/ol\\u003e\"}],\"fulltextSource\":\"\",\"fullText\":\"\",\"funders\":[],\"hasAdminPriorityOnWorkflow\":false,\"hasManuscriptDocX\":true,\"hasOptedInToPreprint\":true,\"hasPassedJournalQc\":\"\",\"hasAnyPriority\":false,\"hideJournal\":false,\"highlight\":\"\",\"institution\":\"\",\"isAcceptedByJournal\":true,\"isAuthorSuppliedPdf\":false,\"isDeskRejected\":\"\",\"isHiddenFromSearch\":false,\"isInQc\":false,\"isInWorkflow\":false,\"isPdf\":false,\"isPdfUpToDate\":true,\"isWithdrawnOrRetracted\":false,\"journal\":{\"display\":true,\"email\":\"info@researchsquare.com\",\"identity\":\"journal-of-iberian-geology\",\"isNatureJournal\":false,\"hasQc\":true,\"allowDirectSubmit\":false,\"externalIdentity\":\"jibg\",\"sideBox\":\"Learn more about [Journal of Iberian Geology](http://link.springer.com/journal/41513)\",\"snPcode\":\"41513\",\"submissionUrl\":\"https://www.editorialmanager.com/jibg/default2.aspx\",\"title\":\"Journal of Iberian Geology\",\"twitterHandle\":\"\",\"acdcEnabled\":true,\"dfaEnabled\":true,\"editorialSystem\":\"em\",\"reportingPortfolio\":\"Springer Hybrid\",\"inReviewEnabled\":true,\"inReviewRevisionsEnabled\":false},\"keywords\":\"ammonites, biostratigraphy, correlations, evolutionary faunal turnovers, migrations\",\"lastPublishedDoi\":\"10.21203/rs.3.rs-4008521/v1\",\"lastPublishedDoiUrl\":\"https://doi.org/10.21203/rs.3.rs-4008521/v1\",\"license\":{\"name\":\"CC BY 4.0\",\"url\":\"https://creativecommons.org/licenses/by/4.0/\"},\"manuscriptAbstract\":\"\\u003cp\\u003eThe transgressive succession of deposits of the late Early Kimmeridgian at Małogoszcz in the south-western margin of the Holy Cross Mts. in central Poland yielded diversified faunas of ammonites. The commonly represented Submediterranean ataxioceratid ammonites include the last members of \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e in the Hypselocyclum Zone and the assemblage of various \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eProgeronia\\u003c/em\\u003e, mostly developed in the Divisum Zone, and associated upwards (Uhlandi Subzone) with aspidoceratids (\\u003cem\\u003ePseudhimalayites\\u003c/em\\u003e). A few typical Mediterranean ammonites (\\u003cem\\u003eNebrodites\\u003c/em\\u003e, \\u003cem\\u003ePresimoceras\\u003c/em\\u003e, \\u003cem\\u003eIdoceras\\u003c/em\\u003e, \\u003cem\\u003eTaramelliceras\\u003c/em\\u003e) are indicative of the Herbichi Zone. The Subboreal ammonites include mostly \\u003cem\\u003eEurasenia\\u003c/em\\u003e, \\u003cem\\u003eInvoluticeras\\u003c/em\\u003e in addition to some \\u003cem\\u003eRasenia\\u003c/em\\u003e and \\u003cem\\u003eRasenioides\\u003c/em\\u003e of the uppermost Cymodoce Zone, corresponding to the Askepta Subzone. The changes in composition of ammonite faunas and comparison with the coeval faunas of other areas of Europe give indications on the evolutionary development of some Ataxiocertidae and Aulacostephanidae at the end of Early Kimmeridgian. The development of the \\u003cem\\u003eCrussoliceras\\u003c/em\\u003e, \\u003cem\\u003eGarnierisphinctes\\u003c/em\\u003e and \\u003cem\\u003eProgeronia\\u003c/em\\u003e, having possibly their roots in the Mediterranean areas, was strictly correlated with the overall transgression and oscillations of sea-level controlled possibly by climatic eccentricity cycles in northern Tethyan shelf. This resulted also in decline of older \\u003cem\\u003eAtaxioceras\\u003c/em\\u003e and its nearby allies. The indigenous lineage of Aulacostephanidae includes the transition from \\u003cem\\u003eEurasenia\\u003c/em\\u003e to \\u003cem\\u003ePararasenia.\\u003c/em\\u003e The development from \\u003cem\\u003eRasenioides\\u003c/em\\u003e to \\u003cem\\u003eAulacostephanoides\\u003c/em\\u003e occurred mostly in the Subboreal areas \\u0026ndash; although some late representatives of \\u003cem\\u003eRasenioides\\u003c/em\\u003e like \\u003cem\\u003eR. moeschi\\u003c/em\\u003e reached the area of study. The existence of an independent lineage leading from \\u003cem\\u003eRasenia involuta\\u003c/em\\u003e to heavily-ribbed \\u003cem\\u003eAulacostephanoides/Aulacostephanus\\u003c/em\\u003e is also suggested.\\u003c/p\\u003e\",\"manuscriptTitle\":\"The ammonite faunas of the upper Hypselocyclum to Divisum zones (Lower Kimmeridgian, Upper Jurassic) at Małogoszcz, Holy Cross Mts., central Poland: their stratigraphical interpretation and evolutionary development\",\"msid\":\"\",\"msnumber\":\"\",\"nonDraftVersions\":[{\"code\":1,\"date\":\"2024-04-19 12:29:52\",\"doi\":\"10.21203/rs.3.rs-4008521/v1\",\"editorialEvents\":[{\"type\":\"communityComments\",\"content\":0},{\"type\":\"reviewerAgreed\",\"content\":\"\",\"date\":\"2024-04-30T12:31:26+00:00\",\"index\":0,\"fulltext\":\"\"},{\"type\":\"reviewersInvited\",\"content\":\"\",\"date\":\"2024-04-16T16:18:54+00:00\",\"index\":\"\",\"fulltext\":\"\"},{\"type\":\"editorInvited\",\"content\":\"Journal of Iberian Geology\",\"date\":\"2024-03-13T17:56:26+00:00\",\"index\":\"\",\"fulltext\":\"\"},{\"type\":\"editorAssigned\",\"content\":\"\",\"date\":\"2024-03-13T03:39:50+00:00\",\"index\":\"\",\"fulltext\":\"\"},{\"type\":\"submitted\",\"content\":\"Journal of Iberian Geology\",\"date\":\"2024-03-12T13:12:15+00:00\",\"index\":\"\",\"fulltext\":\"\"}],\"status\":\"published\",\"journal\":{\"display\":true,\"email\":\"info@researchsquare.com\",\"identity\":\"journal-of-iberian-geology\",\"isNatureJournal\":false,\"hasQc\":true,\"allowDirectSubmit\":false,\"externalIdentity\":\"jibg\",\"sideBox\":\"Learn more about [Journal of Iberian Geology](http://link.springer.com/journal/41513)\",\"snPcode\":\"41513\",\"submissionUrl\":\"https://www.editorialmanager.com/jibg/default2.aspx\",\"title\":\"Journal of Iberian Geology\",\"twitterHandle\":\"\",\"acdcEnabled\":true,\"dfaEnabled\":true,\"editorialSystem\":\"em\",\"reportingPortfolio\":\"Springer Hybrid\",\"inReviewEnabled\":true,\"inReviewRevisionsEnabled\":false}}],\"origin\":\"\",\"ownerIdentity\":\"73c93fd7-33aa-4c59-b6cc-a3f6bb40ebc0\",\"owner\":[],\"postedDate\":\"April 19th, 2024\",\"published\":true,\"recentEditorialEvents\":[],\"rejectedJournal\":[],\"revision\":\"\",\"amendment\":\"\",\"status\":\"published-in-journal\",\"subjectAreas\":[],\"tags\":[],\"updatedAt\":\"2024-09-30T16:15:07+00:00\",\"versionOfRecord\":{\"articleIdentity\":\"rs-4008521\",\"link\":\"https://doi.org/10.1007/s41513-024-00260-y\",\"journal\":{\"identity\":\"journal-of-iberian-geology\",\"isVorOnly\":false,\"title\":\"Journal of Iberian Geology\"},\"publishedOn\":\"2024-09-26 15:58:00\",\"publishedOnDateReadable\":\"September 26th, 2024\"},\"versionCreatedAt\":\"2024-04-19 12:29:52\",\"video\":\"\",\"vorDoi\":\"10.1007/s41513-024-00260-y\",\"vorDoiUrl\":\"https://doi.org/10.1007/s41513-024-00260-y\",\"workflowStages\":[]},\"version\":\"v1\",\"identity\":\"rs-4008521\",\"journalConfig\":\"researchsquare\"},\"__N_SSP\":true},\"page\":\"/article/[identity]/[[...version]]\",\"query\":{\"redirect\":\"/article/rs-4008521\",\"identity\":\"rs-4008521\",\"version\":[\"v1\"]},\"buildId\":\"qtupq5eGEP_6zYnWcrvyt\",\"isFallback\":false,\"isExperimentalCompile\":false,\"dynamicIds\":[84888],\"gssp\":true,\"scriptLoader\":[]}","source_license":"CC-BY-4.0","license_restricted":false}